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Geo-Science Education Journal

Editor-in-Chief Miłosz Andrzej Huber

Maria Curie –Sklodowska University, Lublin, Poland

Redaction residence: Milosz Andrzej Huber, 22 Bartla st, 30-389 Kraków, Poland.

Co-Editors (Thematic Editors)

Tomasz M. Karpiński –biological sciences

University of Medical Sciences, Poznań, Poland

Galina Zhigunova – earth sciences

Murmansk State Humanitary University, Russia

Statistic Editor

Olga Jakovleva, Lublin, Poland

Language Editor

Davor Kredic, Chicago, USA

Scientific Editorial Board

Artem Mokrushin, Apatity, Russia

Victoria Pantyley, Atlanta, USA/Lublin, Poland

Alex Rocholl, GFZ Potsdam, Germany

Nikolai Kozlov, Murmansk State Technical

Uniwersity, Apatity Russia.

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13th Geochronological Conference "Dating of Minerals and Rocks XII"

2st International Conference on Biology and Earth Sciences "Bio-Geo"

UMCS, Lublin, 20-21.10.2016

Geo-Science Education Journal 2016; 2 (Suppl. 1): 1-57

1

PREFACE

This volume contains the conferences program and abstracts prepared by the authors. The authors and

participants are most warmly welcome at Maria Curie-Skłodowska University (UMCS) in Lublin, Poland.

Present conference on Dating of minerals and Rocks XIII joined for the second time Bio-Geo conference,

according to postulates expressed in previous conferences on Dating to include the use of stable isotopes in

bio-geochemical studies.

This joined conference is organized in the 100th Birthday of Włodzimierz Żuk, professor of UMCS, who

constructed the first mass spectrometer in Poland. It is worth to remain that the first all-Polish dating

conference was organized at UMCS in the frame-work of celebration of 50th anniversary of UMCS in

October 1994. At that time the only invited speaker was professor Jan Burchart from the Institute of

Geological Sciences PAN, Warsaw. He was talking on advantages and drawbacks of the K-Ar method.

During this conference we have a great opportunity to provide for all the participants excellent monograph

entitled Isotopic Record of the Earth Past (in Polish) authored by Prof. Burchart and Dr. Jan Kral from

Slovakia.

The Organizing Committee wish to express sincere thanks for help in organization and financial support of

this conference to the Lublin Division of the Polish Physical Society.

Sincerely Yours,

Yours sincerely,

Prof. dr hab. Stanisław Hałas

Dr Tomasz Pieńkos

Dr eng. Miłosz A. Huber



UMCS, Lublin, 20-21.10.2016


2



UMCS, Lublin, 20-21.10.2016

Organizers:

Mass Spectrometry Laboratory, Maria Curie-Skłodowska University in Lublin

Earth Science and Spatial Management Faculty, Maria Curie-Skłodowska University in Lublin

TMKarpiński Publisher

Annales Universitatis Mariae Curie-Skłodowska, sectio “Physica”

Scientific Organizing Committee:

Prof. dr hab. Stanisław Hałas, Chairman

Dr eng. Miłosz A. Huber

Dr hab. Tomasz M. Karpiński

Patrons:

Prof. dr hab. Radosław Dobrowolski, rector of the Sciences and International Cooperation, UMCS

Prof. dr hab. Zbigniew Korczak, dean of Mathematics, Physics and Informatics Faculty, UMCS

Prof dr hab. Sławomir Terpiłowski, dean of Earth Science and Spatial Managment Faculty, UMCS

Prof. dr hab. Jerzy Żuk, head of Polish Society of Physics in Lublin

Prof. dr hab. Mieczysław Budzyński, director of Physics Institute in Lublin, UMCS



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PROGRAM OF CONFERENCES

Hour Speaker Hour

Thursday 20.10.2016. Part I „DATING”

The Institute of Physics UMCS, room 613, 1 Maria Curie –Skłodowska sq.

14:35 Registration

14:50 Opening ceremony

15:10-15:40 Michał Banaś From MS20 to NU Noblesse: a short story of K-Ar dating in

Kraków

15:40-16:10 Zbigniew Czupyt SHRIMP IIe/MC ion microprobe

16:10-16:50 Sylwia Kowalska, Stanisław Hałas, Artur

Wójtowicz, Claus Wemmer

Methodological aspects of K-Ar dating in application to

sedimentary basins thermal history reconstruction

16:50 Prof. dr hab. Jan Burchart Promotion of the monograph “Izotopowy zapis przeszłości

Ziemi” diuring the cofee break

Hall of Physics, 1st floor, (in the framework of the Polish Physical Society Meeting)

17:15-18:00 Monika Kusiak, Dunkley D.J., Lyon I.,

Wirth R., Whitehouse M.J., Wilde S.A.

How far we can get with high-spatial resolution geochronology

for U-Pb dating of ancient rocks

18:00-18:40 Daniel J. Dunkley, M. A. Kusiak, Y.

Hiroi, K. Tani, D. E. Harlov & K.

Shiraishi

Fluids attack the citadel of zircon: some case studies

19:30 Conference Dinner Husar Hotel Restaurant, Ul. Spadochroniarzy 9

Piątek 21.10.2016. Part II „BIO-GEO”

Room 613, 1 Maria Curie –Skłodowska sq.

10:15-11:00 Sándor Kele Clumped isotopes

11:00-11:40 Stanisław Hałas, Tomasz

Pieńkos

Towards determination of multiple sulfur isotope fractionation

11:40-12:00 Coffe Break

12:00-12:40 Zdzislaw Migaszewski , Agnieszka

Gałuszka

Stable S and O isotopes in the Wiśniówka acid mine drainage

water bodies (Holy Cross Moutains, Poland)

https://www.google.pl/maps/place/Wydzia%C5%82+Matematyki,+Fizyki+i+Informatyki+UMCS/@51.2459872,22.5417405,19z/data=!3m1!4b1!4m2!3m1!1s0x47225763ae7d390f:0x90e348332148e2a7

https://www.google.pl/maps/place/Hotel+Huzar/@51.2480699,22.5285562,17z/data=!3m1!4b1!4m2!3m1!1s0x472259dbd86f855d:0x75b26afbb2aa026

https://www.google.pl/maps/place/Wydzia%C5%82+Matematyki,+Fizyki+i+Informatyki+UMCS/@51.2459872,22.5417405,19z/data=!3m1!4b1!4m2!3m1!1s0x47225763ae7d390f:0x90e348332148e2a7



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12:40-13:20 Adrian Pacek, Tomasz

Pieńkos, Stanisław Hałas

A novel ion source for TIMS (used in 7Li/6Li and 39K/41K ratios)

13:20-14:00 Miłosz Huber, Tamara B. Bayanova,

Stanisław Hałas, Emilia Reszczyńska ,

Lesia Lata, Sebastian Skupinski

Sulfur isotopy geochemistry of basic and ultrabasic complexes of

the Kola Peninsula

14:00-15:00 Coffe Break and Poster Session

15:00 Honorable Run of the δ33S- δ34S Mass-Spectrometer and lunch.

Posters index

Author Poster Title

Fedorowicz S., Łanczont M. , Bogucki

A., Standzikowski K., Mroczek P.,

Kusiak J.

Interlaboratory luminescencje dating of meso-pleistocene loesses from Wołyń and

Podole: methodical aspects

Huber M., Bayanova T.B. , Hałas S.,

Reszczyńska M., Lata L. , Skupinski S.

3,7 Ga metamorphosed gneisses from Murmansk, preliminary geochemistry and

isotopic data.

Kusiak M.A., Dunkley D.J.1,,

Sałacińska A., Whitehouse M.J., Wilde

S.A.

Igneous protolites of the Uivak gneiss, preliminary data from the Saglek Block,

Northern Labrador

Hałas S., Pieńkos T., Pelc A.,

Wójtowicz A.

Determination of d33S and d34S on SO2 gas using negative/positive ion mass

spectrometry

Huber M., Lata L. Environmental and pollution characteristics of the Lublin roughcast

Karpinski T.M., Huber M., Lata L. Environmental and pollution characteristic of plants samples from Karkonosze

region, S Poland.

Pieńkos T., Hałas S., Pelc A.,

Wójtowicz A.

A dual inlet and triple collector mass spectrometer for analysis of 33S/32S and 34S/32S isotope ratios

Huber M., Lata L. Environmental moss characteristics from Middle Roztocze (Tomaszów area)

Ciszak A. Fluorination line for extracting of oxygen from minerals

Copyright: © The Author(s) 2016. Geo-Science Education Journal © 2016 Miłosz Huber.

This is an open-access article distributed under the terms of the Creative Commons Attribution

License, which permits unrestricted use, distribution, and reproduction in any medium,

provided the original work is properly cited.

http://journals.mahuber.com/index.php/gsej



UMCS, Lublin, 20-21.10.2016


5

FROM MS20 TO NU NOBLESSE: A SHORT STORY OF K-Ar DATING IN KRAKÓW

Michał Banaś

Institute of Geological Sciences PAS, ul. Senacka 1, 31-002 Kraków

The Laboratory for K-Ar Dating in Kraków was established in the period 1999-2002 based on

the hardware of the CNRS from Strasbourg (Figure 1). The reactor, power supply, controller and

control the spectrometer cold fingers were made at the Maria Curie-Skłodowska University in

Lublin (Figures 2 and 3).

In 2011, the Institute of Geological Sciences PAS received a grant from the National Fund for

New Technologies for the purchase of modern equipment for the laboratory. It was selected the

company's offer NU Instruments "Noblesse 2.1" (Figure 4). A line for gas extraction and

purification of the samples was carried out in Warsaw ITR (Figure 5). The construction of the

laboratory was completed in 2014.

Fig. 1.



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Fig. 2.



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Fig. 3.

Fig. 4.



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Fig. 5.

SHRIMP IIE/MC ION MICROPROBE

Zbigniew Jan Czupyt

Micro-area Analysis Laboratory, Ion microprobe section Polish Geological Institute - National Research Institute, 4

Rakowiecka St., 00-975 Warsaw; e-mail: [email protected]

SHRIMP IIe/MC (Sensitive High Resolution Ion MicroProbe) is a Secondary Ion Mass

Spectrometer (SIMS) that is capable to in situ isotopic and chemical surface analyses of solid targets

[3-5,12-15] A high-energy beam of primary ions is focused onto a small area (from 5 to 30 µm

diameter) on the surface of the target. The ion bombardment sputters atoms and molecules from the

sample. These secondary ions are gathered using electrostatic lenses and transferred to a mass

spectrometer, in which they are separated according to their relative masses. SHRIMP IIe has high

mass resolution which is achieved by the use of a double-focusing mass spectrometer, simultaneous

energy and mass refocusing, with a very large turning radius, magnet radius is 1000 mm and

electrostatic analyzer radius is 1272 mm. That is why instrument has a beam line over 7 m long and

weighs more than 14 tones [18].

The SHRIMP has the high secondary ion transmission necessary to detect trace elements [2, 17] while

maintaining the high mass resolution required to resolve the many molecular interferences that result

from chemically complex minerals. The operation at high transmission with a mass resolution

sufficient to distinguish MREE from LREE oxides, and Pb from Hf dioxides makes the SHRIMP ideal

for low level trace element analyses of geologic materials and U-Th-Pb geochronology [11]. It can be

used for routine measurement of the isotopic composition of, for example, Pb, U, Th, O, S, C, Mg, Ca,

Ti, B, Li, Si and Cr, and the abundances of most elements in the periodic table in geological,

cosmochemical, experimental, or industrial samples.

The SHRIMP IIe/MC has a multicollector which allows subpermil (>0.2 ‰) resolution for isotopic

ratios of C, O, S, and other geologically interesting elements [18]. The use of charge mode

electrometers allows the minor isotopes of 36S, 17O, and 13C in carbonate to be measured using a

Faraday cup instead of an electron multiplier, even though the count rate is only a few hundred

thousand cps in most cases. The use of high-sensitivity hall probes instead of NMR allows for multiple

isotopic systems (O, S in sulfates; O, C in carbonates) to be analyzed in a single analytical spot via

field switching. Stable isotope geochemistry examines the change of the isotopic composition of an

element (H, Li, B, C, N, O, S) produced by chemical or physical processes. SHRIMP measurement of

S isotopes has been used to understand mineral growth mechanisms and genesis, follow changes in

fluid compositions and to constrain the conditions under which rocks and ore deposits form [6].



UMCS, Lublin, 20-21.10.2016


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For isotopically uniform electrical insulators such as zircon, SHRIMP IIe/MC demonstrated capability

to produce replicate oxygen isotopic analyses over a period of several hours that have a standard

deviation of better than 0.2 per mill. SHRIMP IIe/MC main use is U-Pb geochronology. It provides

rapid, reliable dating of micron-scale domains in U-bearing trace minerals at the 1-2% level. The

current technique comprises a measurement of Pb isotopes, U, Th, and uranium oxide species which

are used to calibrate the relative ionization efficiency of U and Pb. SHRIMP analyses are

advantageous in that the fine spatial resolution (in range 20 μm) allows targeting of subgrain domains

in mineral grains with complex growth histories, avoiding inclusions or metamict domains [18]. When

temporal precision higher than 1% is required, the SHRIMP IIe/MC can be used to screen zircon

grains for lead loss, inherited cores, or other problems that may inhibit or complicate TIMS analysis.

The small analytical volume (~1000 cubic microns) allows minimal sample consumption [10]. This

allows for later whole-grain dissolution, combined U - Pb - Th- dating, or the use of multiple in situ

techniques on the same sample, such as SHRIMP IIe U-Pb geochronology, SHRIMP IIe/MC oxygen

isotope analysis, and then laser ICPMS Hf isotopic analysis. SHRIMP IIe has been used for the U-Pb

geochronology of minerals such as zircon, titanite, monazite and xenotime. [ 1, 5, 7-9, 14, 16-17].

REFERENCES:

1. Amelin Y.V. (1998). Geochronology of the Jack Hills detrital zircons by precise U–Pb isotope dilution

analysis of crystal fragments, Chemical Geology, 146: 25-38

2. Black, Lance P.; Kamo, Sandra L.; Allen, Charlotte M.; Davis, Donald W.; Aleinikoff, John N.;

Valley, John W.; Mundil, Roland; Campbell, Ian H.; Korsch, Russell J.; Williams, Ian S.; Foudoulis,

Chris (2004), "Improved 206Pb/238U microprobe geochronology by the monitoring of a trace-element-

related matrix effect; SHRIMP, ID-TIMS, ELA-ICP-MS and oxygen isotope documentation for a

series of zircon standards", Chemical Geology, 205: 1-2

3. Bowring S.A., Williams I.S. (1999). Priscoan (4.00-4.03 Ga) orthogneisses from northwestern

Canada, Contributions to Mineralogy and Petrology, 134: 3-16

4. Clement S. W. J., Compston W., Newstead G. (1977). Design of a large, high resolution ion

microprobe. Proceedings of the International Secondary Ion Mass Spectrometry Conference.

Springer-Verlag.

5. Compston W., Pidgeon R.T. (1986). Jack Hills, evidence of more very old detrital zircons in Western

Australia, Nature, 321: 766-769

6. Eldridge C.S., Compston W., Williams I.S., Walshe J.L. (1987). In-situ microanalysis for 34S/32S ratios

using the ion microprobe SHRIMP, International Journal of Mass Spectrometry and Ion Processes,

76: 65-83

7. Fanning C.M., McCulloch M.T. (1990). A comparison of U–Pb isotopic systematics in early Archean

zircons using isotope dilution thermal ionization mass spectrometry and the ion microprobe. Third

International Archean Symposium, Perth. Extended abstracts volume.

8. Froude D.O., Ireland T.R., Kinny P.D., Williams I.S., Compston W., Williams, I.R., Myers, J.S.

(1983). Ion microprobe identification of 4,100-4,200 Myr-old terrestrial zircons, Nature, 304: 616-618



UMCS, Lublin, 20-21.10.2016


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9. Ireland T.R., Compston W., Heydegger H.R. (1983). Titanium isotopic anomalies in hibonites from

the Murchison carbonaceous chondrite, Geochimica et Cosmochimica Acta, 49: 1989-1993

10. Ireland T.R., Clement S., Compston W., Foster J. J., Holden P., Jenkins B., Lanc P., Schram N.,

Williams I. S. (2008). Development of SHRIMP, Australian Journal of Earth Sciences, 55: 937-954

11. Kinny P.D., Compston W., Williams I.S. (1991). A reconnaissance ion-probe study of hafnium

isotopes in zircons, Geochimica et Cosmochimica Acta, 55: 849-859

12. Matsuda H. (1974). Double focusing mass spectrometers of second order, International Journal of

Mass Spectrometry and Ion Physics, 14: 219-233

13. Moorbath S. (1983). The most ancient rocks? Nature, 304: 585–586

14. Schärer U., Allègre C.J. (1985). Determination of the age of the Australian continent by single-grain

zircon analysis of Mt Narryer metaquartzite, Nature, 315: 52 - 55

15. Stern R.A., Bleeker W. (1998). Age of the world's oldest rocks refined using Canada's SHRIMP. the

Acasta gneiss complex, Northwest Territories, Canada, Geoscience Canada, 25: 27-31

16. Stern R. (2006). A time machine for Geoscience Australia, AusGeo News, 81: 15-17

17. Wilde S.A., Valley J.W., Peck W.H., Graham C.M. (2001). Evidence from detrital zircons for the

existence of continental crust and oceans on the Earth 4.4 Gyr ago, Nature, 409: 175-178

http://www.geology.wisc.edu/~valley/zircons/Wilde2001Nature.pdf

http://www.geology.wisc.edu/~valley/zircons/Wilde2001Nature.pdf



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METHODOLOGICAL ASPECTS OF K-Ar DATING IN APPLICATION TO

SEDIMENTARY BASINS THERMAL HISTORY RECONSTRUCTION

Sylwia Kowalska1, Stanisław Hałas2, Artur Wójtowicz2, Klaus Wemmer3, Zbyszek Mikołajewski4

1Oil and Gas Institute – National Research Institute, Lubicz st. 25 A, 31-503 Kraków, Poland, e-mail: [email protected]

2Mass Spectrometry Laboratory, Institute of Physics, Maria Curie-Skłodowska University Lublin, pl. M. Curie-

Skłodowskiej 1, 20-031, Lublin, Poland 3Sedimentology & Environmental Geology, Geoscience Center, University of Göttingen, Goldschmidtstr. 3, Göttingen,

D-37077 Germany 4PGNiG SA, Geology and Hydrocarbon Production Branch, Poland

K-Ar dating of maximum diagenesis is widely used in geology for thermal history

reconstruction in sedimentary basins. Various research centers give different sizes measurement

error, which should be taken for the results. Usually the reported measurement bias responds only to

standard operating procedure of an individual laboratory. The aim of the present study was to find

out what the real error should be taken into account as the real error when interpreting geological K-

Ar dating results. For this purpose an interlaboratory comparison with the participation of four well-

known laboratories was organized. Three of them are performing measurements by K-Ar method

and one by Ar-Ar method with the use of the capsule technique specially adapted for very fine clay

materials. Following scientists took part in the interlaboratory comparison: Prof. Stanislaw Hałas

and Dr. Artur Wojtowicz from the University in Lublin (K-Ar), Dr. Klaus Wemmer of the

University of Göttingen (K-Ar), Dr. Yakov Kapusta from ACTLAB laboratory in Canada (K-Ar)

and Dr. Chris Hall of the University of Michigan in the USA (Ar-Ar).

The research material consisted of Silurian and Ordovician bentonites from different

boreholes drilled by PGNiG S.A. during hydrocarbon exploration. Interlaboratory comparison was

carried out on three samples. From each sample four different grain fractions <0.02, 0.02-0.05,

0.05-0.2 and 0.2-2 µm were separated at the Institute of Geological Sciences in Krakow. Samples

were splited by quartering, encrypted and sent to the laboratories participating in the comparison.

The determination of the radiogenic argon content in the Mass Spectrometry Laboratory

(UMCS Lublin) was made by use of internal spike method on the modified MS-10 mass

spectrometer. Aliquots from about 40 mg to about 50 mg have been made. Each sample was melted

in the double-vacuum crucible of the argon extraction-purification line in temperature of 1150oC.

Pure 38Ar (produced by the Institute for Inorganic and Physical Chemistry, University of Bern) was

used as spike. Atmospheric argon content was determined by measuring an 36Ar peak in the mass

spectrum. After every measurement cycle blank cycle was performed (at temperature of about

1200oC) to check if all argon had been extracted from the sample. For K-Ar age calculation the

decay constants λe = 0.581·10-10, λb= 4.962·10-10, 40K/K=0.01167% [1] were used. Uncertainty

in K-Ar age was calculated from the extended error propagation formula [2]. The age calculation

was made with the use of K content measured by ACTLAB laboratory.



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Based on the results of interlaboratory comparison, it is clearly visible that the most difficulties

arise from the determination of potassium as for this element greater dispersion of results was

achieved - Fig.1. The results of K-Ar and Ar-Ar dating, summarized in Table 1, show that dating of

diagenetic age is possible for a fraction less than 0.2 µm. All laboratories obtained very similar

results for the three finest fractions. The faction 0.2-2 µm gave distinctly older ages, which proves

an admixture of detrital material. This observation is also confirmed by further studies carried out

simultaneously for several bentonite samples from other boreholes. Comparison of the results

achieved from laboratories taking part in the research clearly indicates that the actual measurement

errors range up to +/- 10 Ma. Significantly younger ages obtained with the Ar-Ar method confirm

the large influence of the Ar escape effect from the very fine grained samples, the so called “recoil

effect" [3] .

5.00

5.50

6.00

6.50

7.00

7.50

8.00

1 2 3 4 5 6 7 8

Actlab - ICP

Getynga

Lab X

Sample no.

K2O

[%

]

Fig.

Fig. 1. The results of interlaboratory comparison – determination of K content.



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Tab 1. The results of interlaboratory comparison - K-Ar and Ar-Ar dating.

Sample Grain size

[µm]

K-Ar [Ma] Ar-Ar

Lublin Getynga Actlab Michigen

1

<0,02 362 349 367 290

0,05-0,02 354 348 282

0,2-0,05 357 351 296

0,2-2 384 356 387 319

2

<0,02 372 365

0,05-0,02 363 359

0,2-0,05 368 364

0,2-2 387 380

3

<0,02 190

147 0,05-0,02 196

0,2-0,05 212

0,2-2 272

REFERENCES

1. Steiger R.H., Jäger E., 1977, Subcommission on geochronology: Convention on the use of decay

constants in geo- and cosmochronology, Earth Planet. Sci. Lett. 36: 359-362.

2. Hałas S., Wójtowicz A., 2014, Propagation of error formulas for K/Ar dating method,

Geochronometria 41: 202-206.

3. Hall C., 2013, Direct measurement of recoil effects on 40Ar/39Ar standards. Geological Society,

London, Special Publications 378: 53-62.



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HOW FAR WE CAN GET WITH HIGH-SPATIAL RESOLUTION GEOCHRONOLOGY FOR U-PB DATING OF

ANCIENT ROCKS

Kusiak M.A.1, Dunkley D.J.1,2 Lyon I.3 , Wirth R. 4, Whitehouse M.J.5, Wilde S.A.2

1Institute of Geological Sciences, Polish Academy of Sciences, Warsaw, Poland; [email protected]

2Department of Applied Geology, Curtin University, Perth, Australia 3SEAES; Material Sciences, University of Manchester, UK

4GeoForschungsZentrum, Potsdam, Germany 5Swedish Museum of Natural History, Stockholm, Sweden

U-Pb dating of zircon (ZrSiO4) is arguably the most versatile geochronological age dating

technique, due to the ability of zircon to survive through the entirety of Earth history and for the

internal check of reliability provided by concordance between the 238U-206Pb (τ1/2~4.5Gyrs) and the 235U-207Pb (τ1/2~0.7Gyrs) chronometers. The greatest innovation was the ability to analyse in-situ on

the tens-of-micron scale, which has allowed us to differentiate and date multiple stages of mineral

growth. Zircon U-Pb isotopic analyses commonly yield discordant data in which 206Pb/238U ages are

younger than 207Pb/206Pb ages due to Pb loss or analysis of mixtures of zircon of different ages.

Such disturbed data commonly lie along a discordia line on the concordia (206Pb/238U versus 207Pb/235U) diagram, which can yield meaningful ages from the upper and lower intercepts with the

Concordia curve. More difficult to explain is the situation where zircon data are reversely

discordant (ie. 206Pb/238U ages are older than 207Pb/206Pb ages). Much research is currently being

undertaken to understand these effects (Kusiak et al., 2013 a,b). It has been discovered that in

zircons from the Napier Complex in East Antarctica, radiogenic Pb was mobilised during high-

grade metamorphism to form metallic Pb nanospheres (Kusiak et al., 2015), typically 20-35nm in

diameter.

Fig. 1. Zircon grain in back-scattered electron image (left), ion image masp of 206Pb and 48Ti showing

inhomogeneous distribution of selected isotopes, transmission electron microscope images showing Pb

nanospheres together with Si-Al phase.

Since the spheres are on the nanometer scale, conventional SIMS analysis, with an analytical spot

size of ca. 15-20μm, can sample variable quantities of the spheres during sputtering and so yield

206

Pb

10μm

10μm T

i

100 nm

100 μm

50 nm

150 nm



UMCS, Lublin, 20-21.10.2016


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scattered apparent 207Pb/206Pb ages within a single analysis. We measured 207Pb/206Pb in individual

Pb nanospheres using the NanoSIMS at the University of Manchester (UK), with an O- primary

beam from a conventional duoplasmatron producing a 100nm wide spot, and on the NanoSIMS of

the University de Pau (France), with a Hyperion O- primary source producing a spot size of 50nm.

The spacing between individual Pb nanospheres is generally greater than 100nm and therefore 207Pb/206Pb can be defined for individual nanospheres. Depth profiling and 3-D reconstructions of

sputtered volumes reveal how the nanospheres are spatially related to one another. A range in 207Pb/206Pb of 0.1 to 0.6 in nanospheres was obtained from different zircons. Modelling of Pb

isotope behaviour on this scale shows how such extreme 207Pb/206Pb isotopic heterogeneity on a

100nm scale within the zircon can arise and be preserved throughout the subsequent history of the

zircon, allowing for a more accurate reconstruction of its true history.

Fig. 2. NanoSIMS images of Pb distribution in the area of 7um in zircon.

REFERENCES:

1 Kusiak M. A. et al. (2013) Amer. J. of Sci. 313, 933-967.

2 Kusiak M. A. et al. (2013) Geology 41, 291-294.

3 Kusiak et al. (2015) PNAS, 112, 4958-4963.



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FLUIDS ATTACK THE CITADEL OF ZIRCON: SOME CASE STUDIES

D. J. Dunkley1,2, M. A. Kusiak1, Y. Hiroi3, K. Tani4, D. E. Harlov5, K. Shiraishi2

1Institute of Geological Sciences, Polish Academy of Sciences, Warsaw, Poland; [email protected]

2National Institute of Polar Research, Tachikawa, Tokyo-to, Japan 3Department of Earth Science, Chiba University, Chiba, Chiba-ken, Japan

4National Museum of Science and Nature, Tokyo-to, Japan 5 GeoForshungsZentrum, Potsdam, Germany

Zircon is an accessory mineral that can preserve within a single crystal multiple records of

growth and modification during geological events. In such complex crystals, isotopic analysis must

be done on micron-scale domains, chosen from interpreted images of polished grain sections

provided by scanning electron microscopy. This is especially the case in rocks produced during

high-grade metamorphism, where zircon interacts with other minerals, and with hydrothermal fluid

and anatectic melt phases. Such interactions are conventionally viewed as dual stage dissolution and

growth processes, producing grains with relict cores and overgrowth rims. However, modification

of zircon during metamorphism also involves chemical re-equilibration via solid-state processes,

either through recrystallization or via coupled dissolution-reprecipitation, especially in the presence

of fluid phases. Zircon textures typical of solid-state modification by hydrous fluids are recognised

from experiment [1] and low/mod-T metamorphic environments, as a result of multiple processes

[2]. Diffusion-reaction (DR), involving partial decomposition of metamict zircon by Ca-Cl-bearing

or other hydrous fluids, can be diagnosed from Ca enrichment, lowered backscattered electron

response, and preservation of primary structures. Coupled dissolution-reprecipitation (CDP),

involving re-equilibration of zircon with fluid or melt, can be diagnosed from reaction fronts with

modified U, Th, Y and/or HREE contents, plus pores and inclusions rich in elements ejected from

primary zircon (e.g., xenotime, thorite, uraninite). At high temperatures (>700°C), modification can

be mediated by hydrous fluids or anatectic melts, but their specific roles can be ambiguous;

especially in migmatites, where both agents are likely to be involved.

Here, three case studies are presented for which the role of fluids can be demonstrated, to help

establish links between reaction textures and agents.

CASE 1: The Karkonosze Pluton of Silesia, Poland, contains magmatic phases produced by the

interaction of evolving S-type granitic magmas with batches of lamprophyric magma. Zircon in

microgranular magmatic enclaves are the product of magma hybridization, being unusually U and

Th-rich, and show further interaction with fluids by alteration along Ca-enriched reaction (DR)

fronts and subsequent repair and re-equilibration through CDP processes, into pristine zircon with

pores and inclusions of xenotime, thorite and other phases. Such zircons record both ca. 315Ma

magmatic growth and ca. 305Ma re-equilibration, the latter recording the time at which late deuteric

fluids released by magma crystallization interacted with the pluton and country rocks [3].



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Fig.1. Backscattered electron image of zircon (left) from a microgranular magmatic enclave, Karkonosze

Pluton, with spot analyses by Sensitive High-Resolution Ion Microprobe (SHRIMP). Centre: element maps

from a 30x50 micron area on the same grain, by field emission electron microprobe. Right: Age data from

SHRIMO spot analyses of magmatic (red), altered (blue) and re-equilibrated (green) domains of zircon.

After Kusiak et al. (2009).

CASE 2: At Skallevikshalsen in East Antarctica, granulite-grade dolomitic marbles contain relics

of ca. 630Ma felsic dykes scapolitised by Cl-rich brines. U-rich magmatic zircon was re-

equilibrated by CDP, as demonstrated by the presence of lobate domains depleted in U, with

inclusions of uraninite). Decomposition of metamict zircon can also be observed along fronts of Ca

enrichment which erode the original magmatic zircon. U-Pb dating resolves two discrete episodes

of fluid activity during high-T metamorphism, at ca. 590 and ca. 540Ma, the latter being confirmed

by ages from uraninite released from zircon during the process [4].

Fig.2. Backscattered electron and cathodoluminescence (CL) images of zircon (top) from skarnified pod in

dolomarble, Skallevikshalsen, East Antarctica, with spot analyses by SHRIMP. Below: REE (left), other

element (centre) and U-Pb isotopic data (right) plots for SHRIMP spot analyses on magmatic (red), 1st stage

metasomatic (green) and 2nd stage metasomatic (blue) domains of zircon.



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CASE 3: Godzilla Mullion, a Miocene oceanic core complex on the edge of the Philippine Sea

Plate, includes Fe-Ti gabbros that were hydrated at and below 800°C, through the injection of

seawater along deeply penetrating faults that also exhumed oceanic lithosphere. Metamorphosed

gabbros and felsic melt veins both contain zircon crystals with Th+U+Y-rich cores, which were

modified by CDP processes into zircon with abundant pores and inclusions of xenotime, thorianite,

britholite and apatite. Re-equilibrated, lower U+Th zircon is younger than unmodified zircon by

less than 1m.y. DR textures are absent, as expected for non-metamict zircon, demonstrating that

neither low-grade alteration nor metamictisation is required to initiate CDP [5].

Fig.3. Backscattered electron and CL images of zircon (left) from metagabbro, Godzilla Mullion. Below left:

element maps from a 30x100 micron area on the same grain, by field emission electron microprobe. Right:

Backscattered electron and CL images of zircon from felsic vein cutting metagabbro. Centre: SHRIMP age

data from magmatic (green), and re-equilibrated (yellow) domains of zircon. Modified after Tani et al.

(2011).

REFERENCES:

1 Harlov & Dunkley (2010) AGU Fall Meeting, abstract V41D-2301.

2 Geisler et al. (2007) Elements 3, 43-50.

3 Kusiak et al. (2009) Geology 37, 1063-1066.

4 Dunkley D. J. (2010) Goldschmidt Meeting, abstract 2692.

5 Tani et al. (2009) Geology 39, 47-50.



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CLUMPED ISOTOPES: THEORY, CALIBRATIONS AND APPLICATIONS

Sándor Kele

Institute for Geological and Geochemical Research, Research Centre for Astronomy and Earth Sciences, Hungarian

Academy of Sciences, Budapest, Hungary, [email protected]

Introduction, history, theoretical base

Clumped isotope geochemistry is a new and dynamically developing research field of

geochemistry, which concerns with the state of ordering of rare isotopes in natural minerals. This

short review briefly introduces the reader to the principles of this method, reviewing the current

state of the art including theoretical basis, calibrations and applications. Clumped isotopes or

multiply-substituted isotopologues are isotopologues that contain two or more rare isotopes (e.g. 13C and 18O) in one molecule and they have unique thermodynamic properties (e.g. bond vibration

frequencies, zero point energies, near-infra-red absorption spectra [1] (Table 1). They were

discussed by the early works of [2] and [3] but until the end of the 80’s they were not studied due to

their extremely low abundances (i.e. lack of proper instrumentation) and lack of appropriate

theoretical framework. Their study started at Caltech (California Institute of Technology, Pasadena,

California) in the early 2000s by John Eiler and his team. [4] showed that clumped isotopes have

unique thermodynamic properties, which can be used to answer long-standing questions of

geochemistry.

Table 1. Stochastic abundances of the twelve isotopologues of CO2 [1].

Mass Isotopologue Relative abundance

44 12C16O2 98.40%

45 13C16O2 1.11%

12C17O16O 748 ppm

46 12C18O16O 0.40%

13C17O16O 8.4 ppm

12C17O2 0.142 ppm

47 13C18O16O 44.4 ppm

12C17O18O 1.50 ppm

13C17O2 1.60 ppb

48 12C18O2 3.96 ppm

13C17O18O 16.8 ppb

49 13C18O2 44.5 ppb

Clumped isotopes are reported by the Δ 47 parameter, which describes the preference of two heavy

(rare) isotopes (e.g. 13C and 18O) to bind to each other. The Δ 47 variable was defined by [4] and [5]

as the difference in per mil (‰) between the measured 47/44 ratio of the sample and the 47/44 ratio

expected for the same sample if its stable carbon and oxygen isotopes were randomly distributed

among all isotopologues (i.e. in case of stochastic distribution) [6]:



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where Ri is the abundance of the minor isotopologues relative to the most abundant isotopologue

with mass 44, and the expected stochastic ratios Ri* are calculated based on the measured

abundance of 13C and 18O in the sample. A more detailed description of the calculation of the Δ 47

variable can be found in [1].

Instrumentation is a key issue in clumped isotope analyses as the measurements require extremely

good precision and reproducibility. Instruments with faraday collectors allowing the simultaneous

measurement of masses 44 to 49 are needed. A commonly used instrument is the Thermo Fisher

Scientific MAT 253 Isotope Ratio Mass Spectrometer, which can be coupled to a KIEL IV

Carbonate Device as at ETH Zürich [7, 8] allowing automated analyses from relatively small

samples (2-3 mg). The Nu Perspective IS mass spectrometer is specially configured to make precise

clumped isotope measurements with exceptional sensitivity and linearity (e.g. at UCLA, Rice

University). There are other mass spectrometers as the MIRA (Multi-Isotope Ratio Analyser) at

University of East Anglia, which is specifically configured for analysis of CO2 isotopologues.

However, there are still challenges in clumped isotope geochemistry as: 1) the method needs

relatively large sample size (2-8 mg); 2) analyses are time-consuming; 3) extremely good precision

and reproducibility is needed; 4) similarly to stable isotopes, disequilibrium processes can affect the

clumped isotope data; 5) there is discrepancy between the published temperature calibrations.

Applications

The method is used in several research fields of geology, including palaeoclimatology,

palaeoceanography, atmospheric research, reservoir geology, geomorphology, structural geology,

diagenesis, biogeochemistry, low temperature metamorphic processes, meteorite research, etc.. Due

to continuous developments, the number of applications is still significantly increasing. The method

has already been applied to a number of materials and questions in geology, for example to soil

carbonates [9, 10], dolomites [11, 12, 13], apatites [14], speleothems and cryogenic cave carbonates

[15, 16, 17], travertines [18], land snails [19], brachiopods [20], foraminifera [21], meteorites [22]

and studies on diagenesis and low grade metamorphism [23]. However, the use of clumped isotopes

is not restricted only to CO2 and gasses like CH4 [24], O2 [25], N2 [26] can be also studied with the

method.

Paleothermometry

In geoscience, one of the most important application of clumped isotopes is paleothermometry. The

main problem of the conventional carbonate-water paleothermometry is that it requires knowledge

of the oxygen isotope composition of the water from which the carbonate precipitated. However,

using the clumped isotope thermometer, the temperature of the carbonate precipitating fluids can be

determined with high precision (±2 °C), based on solely the clumped isotope value (∆47) of

carbonates, as it is based on homogeneous equilibrium (where only components of a single phase is



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involved in the isotope exchange process) and independent of the Δ 18O and Δ 13C values of the

solution [1].

The theoretical basis of the clumped isotope paleothermometer is the proportionality between

observed excess abundance of 13C18O-bonds in carbonate relative to its stochastic distribution and

the carbonate precipitation temperature. Clumping of heavy isotopes (e.g.13C18O-bonds) relative to

stochastic distribution increases with decreasing temperature and vica versa. In practice this means

that the Δ 47 parameter is low at high temperatures (e.g. the Δ 47 of CO2 is 0‰, when the gas is

heated to 1000 °C), high at low temperatures and it is about 0.7‰ for carbonates forming at Earth

surface conditions [6]. The blocking or closure temperature of the method is around 250-300 °C

where the solid-state exchange ceases [27].

Calibrations

The first calibration of the clumped isotope thermometer was obtained by laboratory precipitation

experiments [6] in the 1-50 °C temperature range, which was followed by several studies on

biogenic carbonates (brachiopods, mollusks, foraminifera) and inorganic carbonates (travertines,

diagenetic calcites, pedogenic carbonates, dolomites, etc.). However, discrepancy between the

published calibration curves hamper the use of the clumped isotope thermometer. It was suggested

that the different phosphoric acid reaction temperatures for the conversion of sample carbonate to

CO2 may be one of the main causes of discrepancies [28], but there are arguments against this idea

[29].

Because laboratory calibrations are challenging, naturally precipitated carbonates are an important

source of calibration materials for both the oxygen isotope and clumped isotope fractionation,

provided that temperature and conditions of carbonate precipitation are well known. Most

calibrations based on natural samples are limited to temperatures below 45 °C, while experimental

calibrations can cover wide (e.g. 25-250 °C, [30]) temperature range.

The study of active travertine depositing hot spring systems as well as tufa precipitating karstic

springs are important in understanding the dominant controls on the carbonate-water oxygen isotope

fractionation and on the clumped isotope thermometer. [18] proposed a travertine-based calibration

of the clumped isotope thermometer, which is based on recently forming calcitic and aragonitic vent

and pool travertines, including tufa and cave deposits (Fig. 1). The main advantages of the

travertine-based calibration are: (1) Travertines grow over a wide (6-95 °C) temperature range; (2)

the temperature, pH, and chemistry of the depositing water and deposition rate can be measured in

the field; (3) these carbonates represent mainly inorganic deposits and show no biological vital

effect; (4) they can form different polymorphs of calcium carbonate (calcite, aragonite). The

travertine-based T- Δ 47 relationship is [18]:

Δ47 = (0.044 ± 0.005 x 106) / T2 + (0.205 ± 0.047) R2 = 0.96

Tufa samples and three biogenic samples (bivalve, brachiopod, eggshell) fit well within the error of

the regression, supporting the validity of the travertine calibration also for tufa formed in karstic



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environments and for biogenic carbonates. This calibration is the most robust available calibration

from naturally precipitated inorganic carbonates and it suggests that pH, mineralogy, precipitation

rate have no or only minor effects on the Δ 47–signal of carbonates [18]. Using the travertine-based,

empirically determined calcite–water oxygen isotope fractionation factor, the Δ 18O values of the

travertine and tufa depositing waters can be calculated with more confidence.

Fig.1. Comparison of recently published calibration curves of the clumped isotope thermometer.

The travertine calibration was successfully used for dolomites [12] and gastropods [31] as well

proving its usefulness for other type of carbonates. Newest studies [13] seems to confirm this

hypothesis suggesting that an universal Δ 47 –T may exists across all carbonate-bearing mineral

phases.

S.K. was sponsored by the János Bolyai scholarship, the Hungarian Scientific Research Fund

(OTKA 101664), and the SCIEX postdoctoral Fellowship (ClumpIT; Nr: 13.071-2).

REFERENCES:

1. Eiler, J.M. (2007) Earth Planet. Sci. Lett. 262, 309-327.

2. Urey, H.C. (1947) J. Chem. Soc. 562–581.

3. Bigeleisen, J. and Mayer, M.G. (1947) J. Chem. Phys. 15, 261-267.

4. Eiler, J.M. & Schauble, E. (2004) Geochim. Cosmochim. Acta 68, 4767–4777.



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5. Wang, Z. et al. (2004) Geochim. Cosmochim. Acta 68, 4779–4797.

6. Ghosh et al. (2006) Geochim. Cosmochim. Acta 70, 1439-1456.

7. Schmid, T.W & Bernasconi, S.M. (2010) Rapid. Comm. Mass. Spec. 24, 1955-1963.

8. Meckler, A.N. et al. (2014) Rapid. Comm. Mass. Spec. 28, 1705-1715.

9. Ghosh et al. (2006) Science 311, 511-515.

10. Quade et al. (2007) Rev. in Min. and Geochem. 66/1, 53-87.

11. Ferry et al. (2011) Geology 39/6, 571-574.

12. Millán et al. (2016) J. Sed. Res. 86/2, 107-112.

13. Winkelstern et al. (2016) Chem. Geol. 443, 32-38.

14. Eagle et al. (2010) PNAS, 107/23, 10377-10382.

15. Affek et al. (2008) Geochim. Cosmochim. Acta 72/22, 5351-5360.

16. Daëron et al. (2011) Geochim. Cosmochim. Acta 75/12, 3303-3317.

17. Kluge et al. (2014) Geochim. Cosmochim. Acta 126, 541-554.

18. Kele et al. (2015) Geochim. Cosmochim. Acta 168, 172-192.

19. Zaarur et al. (2011) Geochim. Cosmochim. Acta 75, 6859-6869.

20. Came et al. (2007) Nature 449, 198-202.

21. Tripati et al. (2010) Geochim. Cosmochim. Acta 74, 5697-5717.

22. Guo, W. & Eiler, J.M. (2007) Geochim. Cosmochim. Acta 71/22, 5565-5575.

23. Huntington et al. (2011) J. Sed. Res. 81/9, 656-669.

24. Piasecki et al. (2016) Geochim. Cosmochim. Acta 190, 1-12.

25. Yeung et al. (2012) J. of Geophys. Res: Atmospheres 117/D18306, 1-20.

26. Li et al. (2016) 5th International Clumped Isotope Conference, St. Petersburg, Florida

27. Dennis, K.J. & Schrag, D.P. (2010) Geochim. Cosmochim. Acta 74/14, 4110-4122.

28. Fernandez, A. et al. (2014) Geochim. Cosmochim. Acta 126, 411-421.

29. Defliese, W.F. et al. (2015) Chem. Geol. 396, 51-60.

30. Kluge, T. et al. (2015) Geochim. Cosmochim. Acta 157, 213-227.

31. Grauel et al. (2016) EPSL 438, 37-46.



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TOWARDS DETERMINATION OF MULTIPLE SULFUR ISOTOPE FRACTIONATION

S. Hałas, T. Pieńkos

Mass Spectrometry Laboratory, Maria Curie-Skłodowska University, 20-031 Lublin, Poland

The principal motivation of this study is to apply SO2 gas in the multiple isotope analysis (i.e.

simultaneous analysis of sulfur isotope ratios: 33S/32S , 34S/32S and 36S/32S) of sulfur rather than SF6

gas. The first one can by easily prepared from sulfides [7] and sulfates [4] whilst the second

requires the use of a fluorination line [3, 6] and a mass spectrometer with enhanced resolving

power to resolve isotope peaks 33SF5- from 32SF5

- (masses 128 and 127).

This lecture summarizes the main achievements obtained in our Mass Spectrometry

Laboratory with analysis of electronegative gases such as SF6, SiF4, SO2, CH3Cl, CO2, CO, O2 etc.

Previously described negative ion source bases on the thermal emission from hot metal surface [5].

However, that type source is useful for analysis of the negative ions like SF5-, Cl-, Br-, which are

formed by low energy (~0 eV) electron attachment.

In the patent application [2] we have described a new ion source which can be applied for

analysis of gases requiring much higher electron energy for their generation, of order of ~10 eV.

Yet in our preliminary experiments we have demonstrated useful mass spectra of SO- and S- ions

obtained from SO2 gas for sulfur isotope analysis [1].

Figure 1. Overall view on the 60o magnetic sector mass spectrometer. The dual inlet system is installed at

the front panel. The ion source is on the right side and the collector assembly on the left of the flight tube.

The recording of mass spectra and the analysis of isotope ratios are computer controlled.



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The new ion source differs from the Nier type ion one that the electron beam is replaced by

a filament for a strong electron emission inside the ionization chamber. The former ion repeller

inside the chamber is kept on positive potential with respect to the filament. This significantly

enhances generation both of negative and positive ions in the space along the filament which is

immersed in a uniform magnetic field (5-10 mT) with its vector directed along the filament. The

magnetic field is produced by a small external electromagnet. The ions generated inside the ionizer

chamber are extracted in usual way by an electrostatic lens. It was demonstrated recently that sulfur

isotope analysis is more accurate on positive S+ ions because the ion currents are larger at least by

two orders of magnitude.

The analyzed gas is admitted to the ionizer through separate capillaries connected to the

pneumatically operated changeover valve as described by Halas (1979). The overall view of the

mass spectrometer is shown in Fig. 1.

We thank to Dr. Keith Hackley for donation of old mass spectrometer to UMCS, on the basis of

which we were able to develop the new instrument.

This study was supported by NCN project 2013/11/B/ST10/00250.

REFERENCES:

1. Hałas S., Pieńkos T., Pelc A., Wójtowicz A. (2015) Use of negative ion mass spectrometry for

simultaneous determination of sulfur isotope ratios δ33S and δ34S, Annales UMCS Physica 70 : 77-

82.

2. Hałas S., Pieńkos T., Pelc A., Wójtowicz A. (2016) Patent descriprtions P.416375 and P.417560.

3. Hulston J.R. and Thode H.G. (1965) Cosmic-ray produced S36 and S33 in the metallic phase of iron

meteorites, J. Geophys. Res. 70:4435-4442.

4. Halas S. and Wolacewicz W. (1981) Direct extraction of sulfur dioxide from sulfates for isotopic

analysis, Anal. Chem. 53: 686-689.

5. Pelc A. and Halas S. (2008) Negative ion source for chlorine isotope ratio measurements, Rapid

Commun. Mass Spectrom. 22: 3977-3982.

6. Ono S., Wing B., Johnston D., Farquhar J.,Rumble D. (2006) Mass dependent fractionation of

quadruple stable sulfur isotope system as anew tracer of sulfur biogeochemical cycles, Geochim. et

Cosmochim. Acta 70: 2238-2252.

7. Robinson B. and Kusakabe M. (1975) Quantitative preparation of sulfur dioxide, for 34S/32S

analysis, from sulfides by combustion with cuprous oxide. Anal. Chem. 47:1179-1181.



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STABLE S AND O ISOTOPES IN THE WIŚNIÓWKA ACID MINE DRAINAGE WATER

BODIES (HOLY CROSS MOUNTAINS, POLAND)

Zdzisław M. Migaszewski*, Agnieszka Gałuszka

Jan Kochanowski University in Kielce (Poland) Geochemistry and the Environment Div.

*Corresponding author: e-mail: [email protected]

Acid Mine Drainage (AMD) is typically produced by weathering processes of pyrite,

marcasite (FeS2) and other iron-bearing sulfides, which are induced by mining, mineral processing

or other human activity. In contrast, Acid Rock Drainage (ARD) occurs in oxidizing surficial

environments when unmined sulfide ore deposits or mineralized rock formations are exposed by

geologic processes. Sometimes a collective term Acid Mine Drainage (AMD) or Acid Drainage

(AD) is used when describing both naturally- and anthropogenically-induced processes. The AMD

waters are characterized by the following properties:

Low pH (1.5 – 4.0),

Increased metal(loid) concentrations (0.1 – 500 mg/L);

High sulfate concentrations (500 – 10,000 mg/L);

Low concentrations of dissolved oxygen (<5 mg/L),

Increased suspended solids.

The AMD formation is initiated by oxidation of pyrite and marcasite (FeS2) or other iron-

bearing minerals, including arsenopyrite (FeAsS) and chalcopyrite (CuFeS2), according to the

following simplified reactions:

FeS2 (pyrite) + 3.5O2 + H2O Fe2+ + 2SO42– + 2H+ (1)

FeS2 + 14Fe3+ + 8H2O 15Fe2+ + 2SO42– + 16H+ (2)

The reaction (2) is more effective in generation of hydrogen ion involving ferric iron as an

oxidant. Subsequently, ferrous iron undergoes oxidation to ferric iron (reaction 3) which in turn

either hydrolyzes and precipitates in the form of Fe(OH)3 (reaction 4) or oxidizes pyrite (reaction

2):

Fe2+ + 1/4O2 + H+ Fe3+ + 0.5H2O (3)

Fe3+ + 3H2O Fe(OH)3 + 3H+ (4)

Geochemical studies of AMD waters in the Wiśniówka mining area (Fig. 1), including stable S,

O and H isotope determinations, have been carried out since 2005 [1,2,3]. The principal objective of

these and ongoing studies is to: (i) better understand oxidation processes, (ii) apply characteristic S

and O isotope profiles to pinpoint rock mining and processing operations, (iii) assess a potential

impact of AMD waters on the neighboring surface water systems and farmer’s wells.



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Fig. 1. Localization of acid water bodies in the Wiśniówka area

The stable S and O ratios of these acid water bodies indicate that the principal source of

dissolved sulfates is the oxidation of pyrite. This is evidenced by the presence of negative 34S-SO4

values, which in the Podwiśniówka area are relatively close to the 34S-FeS2 values. Both the

former non-existent pit pond [1] and the present acid pit lake (ongoing study) showed similar 34S-

SO4 signatures: mean of –15.61.5‰ and –15.10.3 ‰, respectively. By comparison, the mean

34S-FeS2 value is –25.42.5‰. This isotope shift toward less negative 34S-SO4 values is induced

by bacterial (dissimilatory) reduction of dissolved sulfate combined with the release of isotopically

lighter H2S, and presumably with subordinate mineralization of carbon-bonded sulfur compounds.

The previous and present geochemical studies have revealed no relationship between the old

and new Podwiśniówka water bodies and the Marczakowe Doły acid and fish ponds, which is also

documented by different chemistry of these waters [3]. Of the three farmer’s wells examined, only

the one located near the Marczakowe Doły fish pond (Fig. 1) reveals a negative 34S-SO4 value (–

12.8‰) as opposed to the others located in two villages of Masłów Drugi and Łąki (+6.4 and

+7.5‰). Moreover, these three farmer’s wells exhibit different 18O-SO4 values, i.e. the farmer’s

well near the Marczakowe Doły fish pond (–2.1‰) vs. the remaining two wells (+1.8‰ and –

0.9‰), respectively.

The preliminary study shows that the Wiśniówka Duża pit sump water is enriched in a 34S

isotope compared to the Podwiśniówka acid water bodies. The 34S-SO4 value varies in the range of

–11.7 to –10.4‰. This may suggest the other generation of pyrite mineralization. However, this

issue needs further studying.

Acknowledgements



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This study was supported by the National Science Center, a research grant #2015/17/B/ST10/02119.

References

1. Migaszewski Z.M., Gałuszka A., Hałas S., Dąbek J., Dołęgowska S., Budzyk I., Starnawska

E., Michalik A. 2009. Chemical and isotopic variations in the Wiśniówka Mała mine pit

water, Holy Cross Mountains (South-Central Poland). Environmental

Geology/Environmental Earth Sciences 57, 29-40.

2. Migaszewski Z.M., Gałuszka A., Hałas S., Dołęgowska S., Dąbek J., Starnawska E. 2008.

Geochemistry and stable sulfur and oxygen isotope ratios of the Podwiśniówka pit pond

water generated by acid mine drainage (Holy Cross Mountains, south-central Poland).

Applied Geochemistry 23, 3620-3634.

3. Migaszewski Z.M., Gałuszka A., Michalik A., Dołęgowska S., Migaszewski A., Hałas S.,

Trembaczowski A. 2013. The use of stable sulfur, oxygen and hydrogen isotope ratios as

geochemical tracers of sulfates in the Podwiśniówka acid drainage area (south-central

Poland). Aquatic Geochemistry 19, 261-280.



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IMPROVED TRIPLE-FILAMENT ION SOURCE FOR TIMS USED IN 7Li/6Li AND 39K/41K RATIOS DETERMINATIONS

A. Pacek*, T. Pieńkos, S. Hałas

Mass Spectrometry Laboratory, Maria Curie-Skłodowska University, 20-031 Lublin, Poland

*[email protected]

Lithium and potassium belong to the first group of the Periodic Table. Their ionization energy is

relatively low, what makes lithium and potassium atoms easily ionizable in the contact with a hot metal

surface of high electronic work function. This is the reason why Thermal Ionization Mass Spectrometry

(TIMS) is convenient method for precise analysis of Li and K isotope ratios. However one should be aware

that there are two essential difficulties in TIMS analysis: mass fractionation effect and cross contamination.

The first one can be overcome by usage of high-mass compounds as a loading form to ion source (e.g.

phosphate, [1]), but the second one has been an unsolved problem so far.

Our improved triple filament ion source (Fig. 1) is equipped with two evaporation filaments

(rhenium) and one ionization filament (platinum/iridium) located parallel between them in front of the

extraction slit.

Figure 1. Triple filament ion source of TIMS with wide ionization filament (Pt/Ir) between evaporation filaments (Rh).

The ion source enable independent control of the temperature at which the sample evaporates and of

the temperature at which ionization occurs to get stable ion current beam. Because of high work function of

platinum, the ionization filament does not require very high temperatures to serve as ionizer. In order to

improve ion source efficiency, we have reconstructed the ion optics systems (Fig. 2). As a result the ion

source produces a stable and high intensity ion beams that allows to analyze of nanogram quantities of

lithium or potassium.



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Figure 2. Schematic diagram of improved triple filament ion source of TIMS. Distances are given in millimeters.

The most important original invention is to use a new concept of ionizing filament i.e. platinum

filament which is wide enough to prevent cross contamination of isotopically different samples loaded on

two separate evaporators. Thus different samples can be measured one after another alternately without

venting the mass spectrometer chamber. The results of measurements of two extremely different potassium

samples are shown in Fig. 3. One is natural sample with R = 13.59 and the second is 41K spike with R =

0.0522, where R is the isotopic ratio R = 39K / 41K. The analysis was conducted for over 100 minutes,

however no symptoms of cross contamination for at least 5 hours of alternate analysis were noticed.

Figure 3. The results of measurements of the isotopic ratio of two extremely different potassium samples loaded at the same time on

different evaporators. The measurements was conducted alternately without venting spectrometer chamber.



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Mass spectra corresponding to the measurement of natural sample and 41K spike sample discussed

above are shown in figures 4 and 5, respectively.

Figure 4. Mass spectrum of K natural with visible trace of 40K peak.

Figure 5. Mass spectrum of 41K spike.

In this approach Li or K are loaded onto evaporation filaments in form of phosphate. Consequently

mass fractionation effect is reduced by the evaporation of relatively heavy molecular species of phosphate

[4]. Phosphate molecules dissociate and ionize at the ionization filament predominantly to the Li+ or K+ ions,

where electric field directs them to the analyzer chamber of the mass spectrometer. Minimizing of mass

fractionation effect is extremely important in the case of lithium – very light element. The values of δ7Li for

the natural samples are determined with achieved reproducibility about a few permil or better. Illustrative



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mass spectrum of Li is shown in Fig. 6. Numerical simulations of the ion beam forming in the ion source are

shown in Fig. 7.

Figure 6. Mass spectrum of Li.

Figure 7. Numerical simulations of the ion trajectories along the ion source. The blue objects are the electrodes whist the green lines

indicate cross-sections of the equipotential surfaces.

This relatively cheap method of lithium and potassium isotope determination requires neither

complicated chemical preparation of the investigated samples, nor large quantities of material. In fact this is

one of the simplest methods, although in comparison to ICP-MS is quite time consuming. We have

demonstrated that our new ion source allows to measure the isotope ratio of potassium with accuracy of half

permil or better. High sensitivity of such analysis is confirmed by the presence of the peak 40K in potassium

spectrum. Possibility of alternate sample-standard analysis may lead to detect the variability of potassium

isotopic ratio in natural samples, which has never been found so far.



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33

REFERENCES:

1. Chan L.-H. (2004), Chapter 6 in: de Groot P. A. (editor), Handbook of Stable Isotope

Analytical Techniques, vol.1, Elsevier, Amsterdam.

2. Moriguti T. & Nakamura E. (1993), Precise Lithium Isotopic Analysis by Thermal

Ionization Mass Spectrometry Using Lithium Phosphate as an Ion Source Material, Proc.

Japan Acad., vol. 69 Ser. B, pp. 123-128.

3. Xiao, Y. K. & Beary, E. S. (1989), High-precision isotopic measurement of lithium by

thermal ionization mass spectrometry Int. J. Mass Spectrom. Ion Processes, vol. 94, pp.

101-114.

4. You C.F. & Chan L.H. (1996), Precise determination of lithium isotopic composition in low

concentration natural samples, Geochim. Cosmochim. Acta, 60: 909–915.

5. IAEA (International Atomic Energy Agency) Analytical Quality Control Services,

Reference Materials Catalogue, 2004 – 2005, Vienna, Austria, 2005.



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34

MICROANALYSIS OF PGE MINERALS IN MONCHEGORSK PLUTON, KOLA

PENINSULA, BALTIC SHIELD

Huber M.1*, Mokrushin A.2, Neradowski Yu.2, Halas S.3, Skupiński S.1

1Geology and Lithosphere Protection Dep., Earth Science and Spatial Management Faculty, Maria Curie –Skłodowska

University, 2d Krasnicka Rd, 20-718 Lublin, Poland, email: [email protected] 2Geological Institute of the Kola Scientific Center Russian Academy of Science, 14 Fersmana St. 184209 Apatity Russia,

3Phicycs Institute, , Maria Curie –Skłodowska University, 4 Maria Curie –Skłodowska Sq.,, 20-031 Lublin, Poland

*-corresponding author.

The selected samples of sulfide ore from mafic intrusion from the central part of Kola Peninsula were

performed using a microanalysis with stable sulfur isotopes and XRF analysis. The sulfide samples were

selected from the main ore-bearing rocks of the layered Monchetundra intrusion. The analyzed sulfides

formed several generations of mineralization in the above mentioned fields associated with primary and

hydrothermal stage of formation of the deposits. Isotopic studies confirm a few consecutive stages of

mineralization, which already was particularly well described in the case of sulfides from Fiodoro-Pansky

deposit. These data were compared with the results of Sm-Nd dating of sulfide mineralization. This is due to

the processes of their formation and also imposed factors metamorphic and hydrothermal processes

occurring in these rocks. The results of geochemical and geochronological studies indicate a

complementarity in the context of determining the mineralization stages. In these rocks was found a PGE

phases like kotulskite, maslovite and sperylite. The gabbroanorthosite (2925 ± 7 Ma) earlier

demonstrated zones of sulphide mineralization with increased Pt and Pd concentrations [5-10].

According to Bayanova et al. [1-5] the ore-bearing intrusions formed earlier in the Kola belt

(Fedorov-Pana and other intrusions, 2530-2450 Ma) and at some later stage in the Fenno- Karelian

belt (2450-2400 Ma). These rocks have massive structure and granoblastic texture with plagioclase,

varies from bytownite to labradorite and mafic minerals represented by amphibole and epidote.

Accessory minerals are represented by zircon, titanite, apatite, and Ti-magnetite. The collected

samples of rocks were analyzed using an optical microscope Leica DM2500P and scanning electron

microscope Hitachi SU6600 with EDS at the Department of Geology and Lithosphere Protection

(UMCS, Lublin, Poland). Inclusion of platinum arsenide (sperrylite,PtAs2) and others PGE phases

has been found in the samples with accompanied sulphides. The stable isotope analysis δ34S from

selected sulfide phases was made in Institute of Physics (UMCS), Lublin, on a dual inlet and triple

collector mass-spectrometer. Studied sulphides in the rock massif Monchegorsk indicate high

volatility isotopic resulting from the coexistence of several generations of sulphides. These minerals

form the structure disintegrating, the sulfur contamination of fluids with different backgrounds

which makes it difficult separations and causes large scatter of test results of the same samples of

rocks. In general, these analyses to demonstrate the following characteristics of samples: Multiple

injection ultrabasic magma in the growing cold rocks which contributes to a certain oscillation of

sulfur isotopes of the primary sulphide phases, multi-stage mineralization (magmatic, secondary

magmatic, hydrothermal, epigenetic) -what is associated sulphides processes metamorphism of

sulfides scale and numerous regional tectonic processes sulfide scale meson micro sulphides rocks

of sulphides also creating structures disintegration contributing to the contamination of sulfur

isotopes. PGE examined phases are located in zones of hydrothermal disintegration and, therefore,



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35

are associated with significantly subsequent processes to the original rock forming a background in

which there was a sulfide ore mineralization and mineralization of PGE.

REFERENCES:

1. Bayanova Т.B.,(2004). Возраст реперных геологических комплексов Кольского

региона и длительность процессов магматизма. С.-Пб.: Наука, 174.

2. Bayanova Т.B., Nerovich L.I., Mitrofanov F.P, 2010. Monchetundrovskiy bazitovyi

massiv Kolskogo regiona: novye geologicheskie i izotopio-vozrastnye dannye, Doklady

Akademii Nauk, 431, 2, 216-222, (In Russian).

3. Elizarova I. R., Bayanova T. B., 2012. Mass-spectrometric REE analysis in sulphide

minerals, J. Biol. Earth Sci. 2 (1): E45-E49.

4. Ekhimova N.A., Serov P.A., Bayanova T.B., 2011. Распределение РЗЭ в сульфидных

минералах и Sm-Nd датирование рудогенеза расслоенных базитовых интрузий

Doklady Akademii Nauk, 436, 1, (In Russian).

5. Hattori K, Krouse HR, Campbell FA, 1983. The start of sulfur oxidation in continental

environments: about 2.2x109 years ago, Science 221; 549-551, DOI

10.1126/science.221.4610.549.Hanski E., Huhma H., Smolkin V.F., Vaasjoki M.,

(1990). The age of the ferropicritic volcanics and comagmatic Ni-bearing intrusions at

Pechenga, Kola Peninsula, USSR Bull. Geol. Soc. Finl. 62, 123-133.

6. Huber M., Halas S., Piestrzyński A., (2009). Petrology of gabroides and isotope

signature of sulfide mineralization from Fedorov-Pansky layered mafic intrusion, Kola

Peninsula, Russia; Geochronometria 33, 19-22.

7. Huber M. Hałas S., Lata L., Mitrofanov F.P., Neryadovski Y.N., Bayanova T.B.,

2014:„Stable isotope results of sulfides from old mafic intrusions in the Kola Peninsula

(N Russia)” JBES, 4(S1): 27-28

8. Kudryshov NM, Mokrushin AV, Mesoarchean gabbroanorthosite magmatism of the

Kola region: petrochemical, geochronological, and isotope-geochemical data . Journal of

Petrology, 19, 2011, 167-182 .

9. Mokrushin A.V., Kudyrashov V.M., Huber M. (2014) „First Discovery of sperrylite in

archean patchemvarek gabroanorthosite (Kola region, Russia)”, , in 12th International

Platinum Symposium, 11-14 August, Yekaterinburg, Russia, 307-308

10. Sharkov EV, Formation of layered intrusions and related mineralization . Scientific

world, 2006. Moscow pp 364 Pozhylienko WI. et al. 2002. Geology of the ore regions in

Murmańsk District, Apatity, 360



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36

INTERLABORATORY LUMINESCENCJE DATING OF MESO-PLEISTOCENE

LOESSES FROM WOŁYŃ AND PODOLE: METHODICAL ASPECTS

Stanisław Fedorowicz 1, Maria Łanczont 2, Andriy Bogucki 3, Karol Standzikowski 2,

Przemysław Mroczek2, Jarosław Kusiak 2

1 Uniwersytet Gdański, Instytut Geografii, Katedra Geomorfologii i Geologii Czwartorzędu, 80-309 Gdańsk,

ul. Bażyńskiego 4 2 Uniwersytet Marii Skłodowskiej Curie, Zakład Geoekologii i Paleogeografii, 20-718 Lublin, Aleja Kraśnicka 2cd

3 Katedra Geomorfologii i Paleogeografii Narodowego Uniwersytetu im. Ivana Franka, 79000 Lwów,

ul. Doroszenka 41, Ukraina

W zachodniej części Ukrainy, występuje zwarta i miąższa pokrywa lessowa. Do kluczowych

profili na tym obszarze należą Wołoczysk, Korsziw, Bojanice usytuowane w odległości od siebie

od 70 do 150 km. Profile te odgrywają ważną rolę w stratygrafii środkowego i górnego plejstocenu

w Europie Środkowej i dlatego wytypowano je do szczegółowych datowań luminescencyjnych.

Wykonano je w 3 polskich laboratoriach (Gdańsk, Lublin, Gliwice). Daty były wykonane metodami

luminescencyjnymi: termoluminescencyjną (TL), optycznie stymulowanej luminescencji (OSL) –

technikami SAR oraz post IR IRSL. Wykorzystano różne rodzaje i frakcje ziaren, najgrubsze

kwarcowe: 90–125 µm (SAR OSL w Gliwicach) i 80-100 µm (TL w Gdańsku), polimineralne

frakcje o wielkości: 45-65 µm (SAR OSL w Lublinie), 45-56 µm (post-IR IRSL w Lublinie) 4-11

μm (post- IR IRSL w Gliwicach). Szczególnie cenne z punktu widzenia porównań są daty uzyskane

dla próbek pobranych z tych samych miejsc i wykonane przez wszystkie 3 laboratoria, jak było w

przypadku profili Korsziw i Wołoczysk. Dodatkowo dla Wołoczyska uzyskano wyniki dla różnych

frakcji ziaren polimineralnych najnowszą metodą post-IR IRSL.

Ramy czasowe formowania sekwencji lessowo-glebowej zostały skorelowane ze stadiami

izotopowo-tlenowymi (MIS). Są one dla obszaru Ukrainy następujące: less L2 tworzył się od 210

do140 ka, gleba interglacjalna S1 – od 140 do75 ka, less L1 – od 75 do kilkunastu ka. W obrębie

lessu zarówno L2 jak i L1 wyodrębnione zostały mniejsze jednostki stratygraficzne dotyczące gleb

interstadialnych.

W profilu Wołoczysk (Wyżyna Podolska) badano część sekwencji osadów obejmujących

dwie jednostki lessowe (L2 i L1 ) rozdzielone pedokomleksem horochiw (S1). Młodszy less L1

rozdziela interstadialną gleba dubno (MIS3), a w obrębie jego części górnej występuję inicjalny

poziom krasyliw (MIS2). W 2010 r. pobrano 13 próbek na datowanie: Gdańsk i Lublin (13 dat TL),

Lublin (13 dat SAR OSL), Gliwice (9 dat SAR OSL). W roku 2014 wykonano dodatkowo dla tych

samych próbek daty metodą post IR IRSL (Lublin – 6, Gliwice - 12). Łącznie dla 13 próbek

uzyskano 53 daty.

W profilu Korsziw (Wyżyna Wołyńska) pełna sekwencja lessowo-glebowa obejmuje warstwy

korelowane z okresem MIS8-2. Wiek luminescencyjny oznaczono dla lessu L2 z poziomem

interstadialnej tarnopolskiej gleby, pedokompleksu horochiw (S1), oraz lessu L1 z śródlessowymi

poziomami glebowymi niższej rangi gleb dubno (MIS3) oraz riwne i krasyliw (MIS2). W 2010 r.

pobrano 31 próbek (31 dat TL – Gdańsk, 28 dat TL – Lublin, 20 dat SAR OSL – Gliwice). Łącznie

dla 31 próbek uzyskano 79 dat.

W profilu Bojanice (zachodnia części Wyżyny Wołyńskiej), badano osady reprezentujące

okres MIS6-MIS2 z podobnym układem warstw lessowych i glebowych jak w Korszewie. Próbki

do datowań pobrano w latach 2007 (14 dat TL – Gdańsk) i 2009 (20 dat TL – Lublin).

Duża liczba (166) wykonanych dat luminescencyjnych daje dobrą podstawę do wniosków

metodycznych i stratygraficznych:

1. Generalnie daty TL są starsze od pozostałych;



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2. Daty OSL są wyraźnie niedoszacowane dla osadów najstarszych;

3. Wszystkie daty gliwickie i lubelskie dla SAR OSL są zaniżone w stosunku do przedziałów

wyznaczonych przedziałami MIS z wyjątkiem subjednostek lessowych i glebowych w

obrębie L1;

4. Żadna zastosowana metoda badawcza nie umożliwiła uzyskania w całości poprawnych dat

w odniesieniu do ram czasowych wyznaczonych przez MIS. To samo stwierdzenie należy

odnieść do różnej rodzajów i wielkości ziaren.

5. Zamiana dużych ziaren kwarcowych 90–125 µm na polimineralne ziarna 4-11 μm to krok w

dobrym kierunku. Powoduje on powiększenie dat OSL i zbliżenie się do przedziału

czasowego wyznaczonego przez MIS 4-5.

6. Najstarsze daty TL dobrze wyznaczają początek depozycji lessu L2 (około 200 ka);

7. Daty uzyskane dla pedocompleksu horochiw (S1) są również zaniżone. Skrajne daty

wskazują, że czas jego tworzenia wynosi około 70 tysięcy lat, co jest zgodne z czasem

wyznaczonym przez MIS5;

8. Subjednostki dubno (MIS3), riwne (MIS2) i najmłodszy krasyliw wyróżnione w obrębie L1

dobrze odpowiadają ramom czasowym wyznaczonym przez MIS;

9. Daty TL gleby dubno z profilu Bojanice mieszczą się w przedziale 45-50 tysięcy lat i

odpowiadają czasowo dacie gleby interstadialnej glinde w Europie Zachodniej;

10. Data uzyskana w spągowej części gleba dubno w Korszewie była porównywalna do daty

uzyskanej w profilu Bojanice;

11. Data uzyskana z próbki pobranej ze stropowej części profilu gleby dubno w Korszewie

uzyskała wiek około 24 tysięcy lat. Najprawdopodobniej daty potwierdzają dwudzielność

tego poziomu, wykazaną w wielu ukraińskich profilach;

12. Daty inicjalnego poziomu krasyliw wskazują, że ostatni jego formowania w minionym

glacjale miał miejsce kilkanaście tysięcy lat temu;

Nie znaleziono dotąd takiej metody ani techniki badawczej która byłaby niezawodna w

datowaniu luminescencyjnym i dawała w pełni satysfakcjonujące wyniki, zgodne z rozpoznaniem

przyrodniczym. Należy w dalszym ciągu poszukiwać nowych sposobów, pamiętając o tym że

procesami sedymentacji w przeszłości sterowały skomplikowane warunki klimatyczno-

środowiskowe, które trudno odtworzyć we wszystkich aspektach ich złożoności, a które miały

pośrednio wpływ na proces wybielania datowanych ziaren.



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38

3.7 GA METAMORPHITE BLOCK FROM MURMANSK: MINERALOGICAL

CHARACTERISTICS

Huber M.1, Bayanova T.B. 2, Hałas S.3, Reszczyńska E.3, Lata L. 1, Skupinski S.1

1Department of Geology and Protection of Lithosphere, , Maria Curie-Skłodowska University, 20 -718 Lublin, 2cd

Kraśnicka rd., Poland, e-mail: [email protected] 2Geological Institute of the Kola Scientific Center Russian Academy of Science, 14 Fersmana St. 184209 Apatity, Russia

3Institute of Physics , Maria Curie-Skłodowska University, M. Curie–Skłodowska Sq. 1, 20-031 Lublin, Poland

The complex of crystalline rocks are located in the city of Murmansk. It is classified by researchers of

the oldest Kolska series [1,7,9,16-18], which are in the vicinity of contact with Murmansk Block deposits.

Studied parametamphites were dated on age of 3.7 Ga, using U-Pb method (unpublished of the Bayanova

data 2015), what makes these rocks among the oldest in the Baltic Shield and on Earth. It is a complex of

rocks that have multiple metamorphism which have numerous intrusive and ultrametamorphic processes

[15].

These rocks are the subject of petrological-geochemical analyzes in order to demonstrate their complex

history and interesting mineralization associated with a number of subsequent secondary processes recorded

in those rocks. The samples were collected in the study area shown in Figure 1. These preparations were

examined using an optical Leica DM2500P microscope with transmitted and reflected light and then tests

were performed using a scanning electron microscope Hitachi SU6600 with an EDS attachment. These

studies were carried out in the Geology and Lithosphere Protection Department at the Earth Sciences and

Spatial Management Faculty at Maria Curie-Sklodowska University (UMCS). In addition, a study was made

of rock with a mass spectroscope at the Institute of Physics, UMCS, in order to determine the composition of

stable isotopes of sulfur in sulphide selected samples. Selected preparations were also investigated using

powder XRD analysis in Geological Institute of the Jagiellonian University in Kraków. In addition, selected

samples were examined by ICP-MS in the Department of Soil Science and Soil Protection (UMCS).

Fig 1. Sketch map with the localization of sampling points in Murmansk region.



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Examined rock samples contain mainly garnet-mica gneisses with plagioclases, quartz sometimes sillimanite

and a range of accessory minerals. Samples of particular interest have signatures of secondary processes.

Recognized garnets constitute solid solutions composed of different individual particles, which may be

associated with crystallization under different conditions. Current plurality of phases such as pyroxenes,

amphiboles, micas point to processes replacing mafic minerals by various stages of metamorphic rocks.

Particularly interesting are the Accessory minerals which can distinguish various types of sulfides including

pyrite, galenite and barite as well as several generations of apatite. In the rocks are both ordinary and apatite

minerals rich in elements of the cerium. The latter indicate that cross-contamination of fluids probably

associated with hydrothermal processes, accompanied by numerous alkaline intrusions associated in the

region of rocks [10-14. 2-6,8]. In these rocks they are also recognized numerous kinematic processes of a

disjunctive and partly plastic tectonic. Underlined are the structures spindle-blasts, and interference zones

and lubricating microflecsural highlighted by staurolite and micas. These structures are present mainly in the

areas of fault ruptures associated Kola region overwhelmed that during the formation probably had an impact

on the surrounding rocks. The evidence of these processes and presence of numerous veins intersecting these

rocks indicates the advanced processes of mobility in the region during its extensive history of existence.

REFERENCES:

1. Bayanova T.B., 2004. Age of Reference Geological Complexes of the Kola Peninsula and

Duriation of the Magmatic Processes: St. Petersburg, Nauka, pp. 174 (in Russian).

2. Boruckiy B.E. 1989; Rock-forming minerals of the high-alkaline complexes [in Russian],

wyd. Nauka, pp. 214.

3. Downes H., Markwik A.L.W., Kemton P.D., Thirlwall M.F., 2001a, The lower crust cratonic

nirth-east Eu: isotopic constraints from garnet granulite xenoliths, Terra Nova 13: 395-400.

4. Downes H., Peltonen P., ManttAri I., Sharkov E.V., 2002, Proterozoic zircon ages from

lower crustal granulite xenoliths, Kola Peninsula, Russia: evidence for crustal growth and

reworking, J. Geol. Soc., London 159: 485-488.

5. Geiger C. A. Armbruster T., 1997, Mn3Al2Si3O12 spessartine and Ca3Al2Si3O12 grossular

garnet: Structural dynamic and thermodynamic properties, American Mineralogist 82: 740-

747.

6. Geiger C.A., 1998. A Powder Infrared Spectroscopic Investigations of Garnet Binaries.

The System Mn3Al2Si3O12–Fe3Al2Si3O12¬–Mg3Al2Si3O12–Ca3Al2Si3O12, Eur. J.

Mineralogy 10: 407-422.

7. Glebovitsky V.A., 2005. Early Precambrian of the Baltic Shield, Nauka, St. Petersburg, pp.

710.

8. Görlich E., 1998 Structural Chemistry of Silicates. Orthosilicates. Polish Academy of

Science, Cracov Branch.



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9. Huber M., 2002. Mineralogical characteristic of garnets from metamorphic rock from the

Lapland Granulite Belt (Kola Peninsula, Northern Russia), Zeszyty Specjalne Pol. Tow.

Min. 20: 272-274.

10. Huber M. 2013. Preliminary characterization of the mineral veins occurring in the Malaya

Belaya Valley in the Khibiny. J. Biol. Earth Sci. 2013, 3 (1): E1-E11.

11. Huber M.A., 2014. Geology of the Kandalaksha part of Lapland Granulite Belt, Kola

Peninsula N Russia, TMKarpinski publisher, pp. 128 (in Polish).

12. Huber M.A., 2015. Mineralogical-Petrography characteristic of the selected alkaline massifs

of the Kola Peninsula, (N Baltic Shield), TMKarpinski publisher, pp. 183 (in Polish).

13. Kogarko L.N., Kononova V.A., Orlova M.P., Woolley A.R. 1995. Alkaline Rocks and

Carbonatites of the World. Part 2: Former USSR, Chapman & Hall, London, p. 226.

14. Kukharenko AA, Orlova MP, Bulakh AG, Bagdasarov EA, Rimskaya-Korsakova OM,

Nefedov EI, et al. 1965. The Caledonian Complex of Ultrabasic Alkaline Rocks and

Carbonatites of the Kola Peninsula and North Karelia (in Russian), Nedra, Moscow, p. 772.

15. Miashiro A., 1994. Metamorphic Petrology, N.Y. University Press, pp.404.

16. Mitrofanov F. P, Balashov J. A. (ed.) 1990. Geochronology and genesis of layered basic

intrusions, volcanites and granitic gneisses of the Kola Peninsula, Autoreferat, Russ. Acad.

Sci., Apatity.

17. Mitrofanov AF. 2000. Geological characteristics of Kola peninsula. Russian Academy of

Science, Apatity, pp. 166.

18. Pozhylienko W.I. (ed.) 2002. Geology of the ore regions in Murmańsk District. (in Russian),

Apatity, p. 360.



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41

IGNEOUS PROTOLITHS OF THE UIVAK GNEISS, PRELIMINARY DATA FROM THE

SAGLEK BLOCK, NORTHERN LABRADOR

Kusiak M.A.1, Dunkley D.J.1,2, Sałacińska A.1, Whitehouse M.J.3, Wilde S.A.2

1Institute of Geological Sciences, Polish Academy of Sciences, Warsaw, Poland; [email protected] 2Department of Applied Geology, Curtin University, Perth, Australia 3Swedish Museum of Natural History, Stockholm, Sweden

The Saglek block in northern Labrador is part of the Nain Province, which forms the

westernmost part of the North Atlantic Craton (Fig.1). It is one of the few regions on Earth

where early Archean crust is preserved. It is

bound by the Paleoproterozoic Torngat

Orogen to the west and, before break-up, was

contiguous with the early Archean Amîtsoq

gneisses of eastern Greenland.

The block comprises gneisses regionally

metamorphosed to granulite-facies at ca.

2.74 Ga and/or amphibolite-facies at ca. 2.70

Ga [1]. Outcrop is dominated by two suites of

metaigneous gneisses: the Uivak I suite (>3.6

Ga), comprising fine to medium-grained

tonalite-trondhjemite -granodiorite (TTG)

gneisses, and the less extensive Uivak II

augen gneiss (ca. 3.4 Ga), consisting of Fe-

rich porphyritic granodiorite and diorite [2, 3].

The Uivak suites are tectonically juxtaposed

and interlayered with supracrustal

assemblages, along with several generations

of felsic pegmatite. Based on the zircon

dating, the presence of enclaves or tectonic

intercalations of pre-Uivak I felsic crust have

been proposed, such as the monzonitic ca. 3.95 Ga Nanok Gneiss [4] and the tonalitic ca.

3.9 Ga Iqaluk Gneiss [5].

Samples of Uivak gneiss were collected and examined from various localities around the

Saglek block (Fig.1). Intrusive relationships were observable in the Uivak gneiss in low-

medium strain domains in the field, including at Tigigakyuk Inlet, where the Nanok gneiss

was first ‘identified’.

Fig.1. Sample locations – Saglek Block, Nain

Province (Labrador Peninsula). Red circles –

samples localities.



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42

Preliminary U-Pb isotopic dating of zircon from three samples, two possible candidates for

Nanok gneiss (Fig.2A&B) and a metapelitic gneiss (Fig. 2C), was done by ion microprobe

at the John de Laeter Centre, Curtin University (Perth, Australia) and the Natural History

Museum (Stockholm, Sweden).

Con

cordant age data obtained from zircon cores with characteristic igneous growth zoning fall

within the interval 3.67-3.76 Ga (Fig. 3A, B, D), consistent with age estimates for the

protoliths of Uivak I gneiss by Schiøtte et al. [7], rather than the older ‘Nanok’ gneiss.

Monazite grains from the metapelite yield metamorphic age of 2.71 Ga (Fig.3C). Older

ages comparable to those found by Krogh & Kamo [1] (3.81 Ga and 3.99 Ga) and

Collerson [3] (3.91Ga) were not obtained.

Fig.2. Samples analysed in this study: (A) Tigigakyuk Inlet, sample L1440, felsic orthogneiss;

(B) Big Island, sample L1443, felsic orthogneiss; (C) Shuldham Island, sample L1450,

metapelite.

A. B. C.

A. B.

C. D.

Fig.3. SHRIMP monazite (A) & (C) and zircon (B)& (D) ages for gneisses and metamorphic schist.



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43

The granodioritic to tonalitic compositions of the orthogneiss samples (L1440, L1443) and

mineralogy (mostly plagioclase and quartz, with minor K-feldspar and biotite, and

accessory zircon and apatite) are consistent with published descriptions of Uivak I Gneiss

[3]. Although the lack of older data does not eliminate the possibility of the existence of an

older ‘Nanok’ gneiss, it supports interpretations that the older ages are from inherited

zircon in younger Eoarchean protoliths.

This research is conducted thanks to the grant for MAK by a Polish National Science Centre; NCN

(nr 2014/15/B/ST10/04245) and funds to MJW from the Knut and Alice Wallenberg Foundation and

the Swedish Research Council. Field work was carried out with the permission and support of

Parks Canada and the Nunatsiavut Government.

REFERENCES:

1. Krogh TE. & Kamo SL. (2006) Geological Society of America Special Papers, 405:91-103.

2. Collerson KD. & Bridgwater D. (1979) Trondhjemites, dacites and related rocks. 205-273.

3. Collerson KD. (1983) Lunar and Planetary Institute Technical Report 83(03): 28-33.

4. Regelous M. and Collerson K.D. (1996) Geochimica Cosmochimica Acta 60:3513-3520.

5. Shimojo et al. (2016) Precambrian Research 278: 218-243.

6. Bridgwater and Collerson K.D. (1976) Contributions to Mineralogy and Petrology 54: 43-59

7. Schiøtte et al. (1989) Canadian Journal of Earth Science 26: 2636-2644.



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44

ENVIRONMENTAL AND POLLUTION CHARACTERISTICS OF THE LUBLIN

ROUGHCAST

Huber M. *, Lata L.

Geology and Lithosphere Protection Dep., Earth Science and Spatial Management Faculty, Maria Curie –Skłodowska

University, 2d Krasnicka Rd, 20-718 Lublin, Poland, email: [email protected], *Corresponding author

Lublin, are the county town of the middle ages. The first houses built in this place already in the early

Middle Ages [2-6]. During the Renaissance falls flourishing city, which is shown in the numerous

monuments including churches and laity. In later centuries, particularly during the partitions Lublin becomes

a provincial town, and in the twentieth century recover again the importance of the regional town and passes

a number of changes[1]. This significantly improves the use of stone in the architectural details. At the time

of socialism in Lublin housed various manufacturing plants, most of which did not withstand political

changes. In Lublin, there are numerous examples of the use of diverse stone in the details of architecture and

these rocks respond differently to destructive factors related to human activity. Sampled within the old city

were subjected to observation of corrosion. For this purpose, we performed field studies involving the

making observations architectural details that helped distinguish several types of corrosion and lesions

associated with human activity (figure 1). Collected samples walls were observed with an optical microscope

Leica DM2500P reflected light. Further tests were carried out in the micro using a scanning electron

microscope of Hitachi SU6600 snap EDS under low vacuum. These studies were performed in the

Department of Geology and Protection of Lithosphere UMTS. Analysed samples were tested for the

presence of metals emissions related to the use of methods of ICP-MS and ASA in the Department of Soil

Science and Soil Protection UMCS.

Fig 1. The sketch (from Google maps) of the centre of Lublin with samples localization.

The chemical composition of the roughcasts samples showed a present of some metals such as lead,

chromium and other. It is also present a carbonate, sulfate precipitates and mosses . There are a processes of

destruction in some houses. It is also present in some samples a dissolved compounds (enrichment Mn, Fe)

and crystallization slots plaster. In the center of city is also present a carbonates (in these houses is a carbon

heating), Some metallic additions are corresponded with roof corrosion processes (eg. The Cracow Gate,

which has a roof made of copper plates). In conclusion, the largest source of pollution in Lublin are localized

on the main streets and close proximity in to the city center.



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45

REFERENCES:

1. Huber M., Mroczek P. (2012). Kamień w architekturze Lublina na przestrzeni wieków,

Biuletyn PIG 448; 2012, 441-450

2. Gawarecki H. (1974) O dawnym Lublinie. Szkice z przeszłości miasta. Wyd. Lubelskie,

Lublin.

3. GawareckiH., GawdzikC. (1964). Lublin krajobraz i architektura. Arkady, Warszawa.

4. Menclt T. (1974). Dzieje Lubelszczyzny .PWN, Warszawa

5. Rozwałka A. (1997).— Lubelskie wzgórze staromiejskie w procesie formowania

średniowiecznego miasta. Wyd. UMCS,-Lublin

6. Rozwałka A., Niedźwiadek R., Stasiak M. (2006). Lublin wczesnośredniowieczny: studium

rozwoju przestrzennego. Fundacja na Rzecz Nauki Polskiej. Wyd. Trio, Warszawa.



UMCS, Lublin, 20-21.10.2016


46

ENVIRONMENTAL AND POLLUTION CHARACTERISTIC OF PLANTS SAMPLES

FROM KARKONOSZE REGION, S POLAND ROUGHCAST

Karpinski T.M.1*, Huber M.2, Lata L2

1Poznań University of Medical Sciences, Department of Medical Microbiology, Wieniawskiego 3,

61-712 Poznań, e-mail: [email protected] 2Geology and Lithosphere Protection Dep., Earth Science and Spatial Management Faculty, Maria Curie –Skłodowska


Sudeten are located in the south-western part of the largest Polish acting within the limits of our

country area where outcrop igneous and metamorphic. They represent a larger portion of the Bohemian

Massif [2,3,8,5]. These formations are often uneven-aged rocks in contact with each other in a tectonic

which is associated with mosaic nature of these mountains. There are exposed rocks of multistage rocks from

Precambrian in Sowiogórski terrain, Śnieżnik Massif and Izera Massif gneisses [1,8], to the youngest cells of

Neogene–volcanic rocks [8]. These mountains are built mostly of rock folded in Hercynian orogeny,

rejuvenated block the movements of Alpine [1,2,3]. Relevant to this discussion is the intrusion of granitoide

rocks of the Karkonosze Mountains, breaking into a metamorphic gneiss of Izera and complex rock

Leszczyniec units built with hornfelses, schists and amphibolites, with the subsequent processes he has

contributed to the mineralization in these mountains [6,7]. Rock samples were taken in the Karkonosze

Mountains, in the vicinity of the Sowia Valley, Skalny Stół, Śnieżka Valley Łomniczka, area of Szklarska

Poreba and Karpacz in 2015 with the knowledge and consent of the authorities of the Karkonosze Mountains

National Park. Preparations were made of rocks and dry up mosses collected in the course of fieldwork.

These samples were examined using a Leica DM2500P polarizing microscope in transmitted and reflected

light and then the micro involving scanning electron microscope Hitachi SU6600. Rock samples were tested

in addition to the participation of X-ray fluorescence spectrometer Epsilon 5 XRF PANalytical. Comp plant

were reviewed by ICP-OAS. Microscopic and spectroscopic studies were performed in the Department of

Geology and protection of the Lithosphere in the Faculty of Earth Sciences and Spatial UMCS. The samples

investigated by ICP-OAS examined in the Department of Soil Science and Soil Protection UMCS. Results of

analyses have been developed using Microsoft Excel and Surfer. Examined samples of bedrock have some

variation characteristic of igneous and metamorphic rocks. Particularly interesting is the mineralization of

metals, which is represented by a variety of ore minerals. They can penetrate into the soil and the plants

further contributing to the accumulation. The investigated plants show relatively low metal content, and the

small quantities of iron, titanium and manganese. It is also associated with a relatively contaminated area

which are Sudety. Some of Zn, Ni, Cu may be related to rock ore mineralization, as noted only in a two

important things arsenic. Karkonosze Mountains is an area with very interesting geological structure and

sculpture associated with numerous geological processes and windy. Occurring within the study sites rocks

are mainly granitoids, metamorphic rocks cover Karkonosze granite such as gneiss, schist, hornfelses. These

rocks have relatively similar to each other mineral and chemical composition, differing only and additions of

accessory and ore minerals. The area of the Karkonosze Mountains is the Karkonosze National Park, which

is a protected zone. The result is that in the area of the Karkonosze Mountains industry is very limited. This

affects the quality of the air. Environmental conditions and the quality of the substrate contribute to the

contamination studied mosses. These, however, are relatively small. Any admixture of metals are closely

connected with the geological substrate.



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47

REFERENCES:

1. Cymerman Z.,(1997), Czy istnieją różnice pomiędzy Sudetami Zachodnimi a Wschodnimi?,

PTMin –Prace Spec., Vol.9, p. 77-79

2. Cymerman Z.,(2000), Tektonika ucieczkowa i kliny terranowe Masywu Czeskiego, Przegląd

Geologiczny, vol. 48, 4, p.336-344

3. Dallmeyer R. D.& FrankeW.& Weber K., (1995), “Pre-Permian Geology of Central and

Eastern Europe, Springer

4. Kryza R.,(1997), Dolnopaleozoiczne ortognejsy w Sudetach: Łuk magmowy, czy ryft

kontynentalny?, PTMin –Prace Spec., Vol. 9, p. 116-119

5. Mazur S.,(1998), Zarys budowy geologicznej masywu Karkonosko –Izerskiego i jego

pozycja obrębie Waryscydów środkowej Europy, PTMin –Prace Spec., Vol.11, p. 31-41

6. Mochnacka K.,(1982), Mineralizacja polimetaliczna wschodniej osłony metamorficznej

granitu Karkonoszy i jej związek z geologicznym rozwojem regionu, Biuletyn Instytutu

Geologicznego, 341, in: Z badań geologicznych regionu dolnośląskiego, vol. XXV

7. Mochnacka K.,(2000), Prawidłowości wykształcenia mineralizacji kruszcowej w

metamorficznej osłonie granitu Karkonoszy –próba powiązania ze środowiskiem

geotektonicznym, PTMin –Prace Spec.,Vol.16, p. 169-190

8. Oberc J.,(1972), Blok Karkonosko –Izerski, Budowa geologiczna Polski, vol .4, in:

Tektonika, part 2, Sudety, Wyd. geologiczne , p. 86-111



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48

A DUAL INLET AND TRIPLE COLLECTOR MASS SPECTROMETER FOR ANALYSIS

OF 33S/32S AND 34S/32S ISOTOPE RATIOS

Pieńkos T., Hałas S., Pelc A., Wójtowicz A.

Mass Spectrometry Laboratory, Institute of Physics, Maria Curie-Skłodowska University, Lublin, Poland

This poster summarizes the properties of recently developed instrument for isotope analysis of 33S/32S and 34S/32S isotope ratios on SO2 gas in the Mass Spectrometry Laboratory [1,2]. So far such

triple-isotope analysis was possible only on SF6 which is difficult to prepare quantitatively from

natural samples. The new possibility offers a newly designed ion source which generate sufficiently

strong ion currents of isotope species 32S, 33S and 34S in the negative as well as in positive mode.

The ion currents of the positive isotope species are detected by three Faraday cups and high-ohm

resistors with resistances of 1, 100 and 10 giga-ohms, respectively. The triple collector assembly is

shown in Fig.1, it is installed on a rotatable CF 63 flange. The resolving slits are located in the focal

plane.

Fig. 1. Triple collector assembly for collection of 32, 33 and 34 ion beams installed on rotatable CF 63

flange.

It is important to have SO2 samples well purified from volatiles which eliminates O2 interference at

mass 32 peak. The UHV in the flight tube of mass spectrometer should be free of water molecules



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49

(H2O, HO and O ions), otherwise the interference at mass 33 may occur from SH ions. When these

conditions are fulfilled, then the observed respective peak ratios are close to 32S/34S = 22.5 and 34S/33S = 5.6 for laboratory working standard.

A great advantage of the isotope analysis on S+ instead of SO+ or SO2+ is that there is no need to

keep constant oxygen isotopic composition in the SO2 gas. Usually sulfide and sulfate samples

have different oxygen, but it doesn’t matter in the case of analysis in S+.

The achieved precision (1σ) on positive ion beams was 0.03‰ and 0.01‰ for δ33S and δ34S,

respectively. The details of the design of the ion source, vacuum system and electronic controllers

are presented in the poster.

We thank to Dr. Keith Hackley for donation of old mass spectrometer to UMCS, on the basis of

which we were able to develop the new instrument.

This study was supported by NCN project 2013/11/B/ST10/00250.

REFERENCES:

1. Hałas S., Pieńkos T., Pelc A., Wójtowicz A. (2015) Use of negative ion mass spectrometry

for simultaneous determination of sulfur isotope ratios δ33S and δ34S, Annales UMCS

Physica 70 : 77-82.

2. Hałas S., Pieńkos T., Pelc A., Wójtowicz A. (2016) Patent descriprtions P.416375 and

P.417560.



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50

ENVIRONMENTAL MOSS CHARACTERISTICS FROM MIDDLE ROZTOCZE

(TOMASZÓW AREA)

Huber M.* , Lata L.

Geology and Lithosphere Protection Dep., Earth Science and Spatial Management Faculty, Maria Curie –Skłodowska


In the spring of 2016 years they have been carried out field work within Middle Roztocze covering

cities such as Susiec, Nowiny, Ulów, Kunki, Krasnobród, Huta Różaniecka. Roztocze is a strip of hills,

which are located in an arc between Upland Lublin and Sandomierz Basin. In the course of its formation

(mainly in the Mesozoic and Neogene, as called. Climactic part of the Metacarpathian Embankment) it was

initially subjected to movements subsidention then elevating movements of Alpine orogeny in the form of a

block of a framework [3, 10, 12, 13, 15]. Carrying mites was held evenly dividing the entire area into

individual blocks [2, 4, 11]. In the ground mites are therefore chalk cliffs (mostly marl and bedrock Late

Cretaceous –mastricht, [9]) and on the rocks arrears rocks included in the Neogene. Neogene is represented

by sands and sandstones and organodetritic limestones and reef, which were at that time deposited during

marine transgression in Baden and Sarmat [1, 7, 11]. The youngest link marine sedimentation and land are

numerous sandstones and found the petrified tree trunks that had been created in conditions resembling the

current wetland cypress forests in brahical environment [1, 4,5,6, 8,11,14]. In later periods followed by

erosion that removed a large part of the Miocene deposits especially in the middle Roztoczu [1,11].

Examined rock samples show a typical variety of this area. They are both the chalk cliffs, Neogene and

Pleistocene. The latter are associated with the formation of the covers of origin glacial and periglacial where

there have to redeposition crumbs older songs sedimentary rocks and crystalline and aeolian sediment

formed in the periglacial conditions. Demonstrated a number of admixtures of chlorine, sulfur, potassium

and other elements resulting from surface surveys in the micro may indicate a dust adsorbed on these plants.

It can be that its origin is associated with fertilizers which are commonly used in the agricultural area. They

found a small metal content in the analyzed samples were the lowest among all examined in this study

sample which indicates a very clean environment prevailing in the mite. Small quantities of Zn and Pb

detrital limestones of the Miocene (as As, Ti) may be associated with the activity of hydrothermal processes

that accompanied hauling metacarpathian blocks shaft at the time of the formation of hills mites. Small

quantities of manganese and iron noted Krasnobrod of mosses are characteristic of the rocks contained in the

substrate in which these metals are common. Some dopant elements found on the surface of these products

may be associated with intensive livestock farming in this region. Moss samples examined by means of ICP -

OAS metal content, have a relatively high degree of purity of all the analyzed samples in this study. This is

due to the lack of industry in the vicinity of the study and a low background metal found in rocks of the

substrate.



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51

REFERENCES:

1. Areń B., 1959, Wyniki badań na odcinku Roztocza Lubelskiego w latach 1956-1957, Prz.

Geol., 7,1,10-13.

2. Buraczyński J., Natężenie erozji wewnętrznej i erozji gleb na Roztoczu Gorajskim: Zeszyty

Probl. Post. Nauk Roln., 193, Warszawa 1977

3. Cieśliński S., Rzechowski J., Mapa geologiczna podłoża czwartorzędu Roztocza między

Tomaszowem Lubelskim a Hrebennem. Tektonika roztocza i jej aspekty

sedymentologiczne, hydrologiczne i geomorfologiczno - krajobrazowe. Lublin 1993

4. Harasimiuk M., Budowa geologiczna i rzeźba Roztoczańskiego Parku Narodowego [w:]

Harasimiuk M., Krawczuk J., Rzechowski J. (red.), Tektonika Roztocza i jej aspekty

sedymentologiczne, hydrogeologiczne i geomorfologiczno-krajobrazowe, Lublin 1993

5. Heflik W., 1996, Badania skrzemieniałych pni drzew z Roztocza. Prace Muz. Ziemi, 44;

127-130.

6. Huber M., Zych Ł., Wstępna petrologiczna charakterystyka skrzemieniałych pni drzew z

Siedlisk, [w:] Harasimiuk M., Brzezińska-Wójcik T., Dobrowolski R., Mroczek P.,

Warowna J., „Budowa geologiczna regionu lubelskiego i problemy ochrony litosfery, wyd.

UMCS 2007, ss. 121-126.

7. Jaroszewski W. Sedymentacyjne przejawy mioceńskiej ruchliwości tektonicznej na

Roztoczu Środkowym. Prz. Geol. tom 25, nr 8-9 Warszawa 1977

8. Kłusek M., 2004: Mioceńskie drewno z Roztocza (Polska południowo –wschodnia),

Geologia 30, 1, 23-31

9. Krassowska A., Kreda między Zamościem, Tomaszowem Lubelskim a Kryłowem. Inst..

Geol. Biuletyn 291. Warszawa 1976

10. Maruszczak H., 2001, Skamieniałe szczatki drzew lasu mioceńskiego na roztoczu (Polska

SE i Ukraina NW). Prz. Geol., 49, 6; 532-537.

11. Musiał T., Litologia i właściwości surowcowej wapieni miocenu Roztocza, Rozprawy

Uniwersytetu Warszawskiego w 265. Warszawa 1987

12. Ney R., Piętra strukturalne w północno - wschodnim obramowaniu zapadliska

przedkarpackiego, Prace Geol. PAN Oddz. W Krakowie t. 9/2 Warszawa-Kraków 1969

13. Pożaryski W., Obszar świętokrzysko - lubelski, [w:] Budowa geologiczna Polski, IV,

Tektonika cz. I. Warszawa 1974

14. Trejdosiewicz J., Pamiętnik fizjograficzny, zeszyt drugi tom III - IV 1884 Wyd.

Geologiczne, Warszawa 1955

15. Żelichowski A., Rozwój budowy geologicznej obszaru między Górami Świętokrzyskimi i

Bugiem. Biul. Inst. Geol. 263 Warszawa 1972



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52

FLUORINATION LINE FOR EXTRACTING OF OXYGEN FROM MINERALS

Ciszak A.

Mass Spectrometry Laboratory, Institute of Physics, UMCS, pl. Marii Curie-Skłodowskiej 1, 20-031 Lublin, Poland e-

mail: [email protected]

Linia fluorynacyjna (pierwotnie nazwana linią krzemianową) została skonstruowana przez

prof. S. Savina z CASE w Cleveland, USA. W wyniku porozumienia prof. J. Środonia i prof. S.

Savina linia ta została sprowadzona do Polski do Instytutu Nauk Geologicznych PAN w Warszawie

a następnie przekazana do Zakładu Spektrometrii Mas w Instytucie Fizyki Uniwersytetu Marii

Curie-Skłodowskiej w Lublinie. Linia fluorynacyjna z pewnymi modyfikacjami została przeze mnie

złożona pod kierownictwem i z pomocą

prof. dr hab. S. Hałasa i jest gotowa do pierwszych testów.

Fig 1. Linia fluorynacyjna

Zasadniczą rolą linii fluorynacyjnej jest ekstrakcja tlenu w postaci cząsteczkowej O2 z minerałów

zawierających w swoim składzie tlen takich jak krzemiany, tlenki, fosforany i woda. W związku

z tym linia z krzemianowej zmieniła swoją nazwę na linię fluorynacyjną. Proces ekstrakcji tlenu

polega na ogólnej reakcji:

M2SiO4 + 4F2 → 2MF2 + SiF4 + 2O2

Próbka minerału ogrzewana jest w obecności czystego fluoru F2 w temperaturze 450 - 750 °C w

kolbie niklowej. Otrzymany w wyniku tej reakcji tlen poddawany jest analizie izotopowej na

spektrometrze mas. Analiza izotopowa na gazie O2 pozwala na określenie pełnego składu

izotopowego 16O, 17O oraz 18O. Dzięki analizie izotopów tlenu można określić genezę złóż

mineralnych, temperaturę wody, w której wytrącała się krzemionka lub wzrastały kryształy kwarcu

a także odtworzyć zmiany klimatyczne na Ziemi.



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Outline of Professor Włodzimierz Żuk (1916 – 1981) life

Sylwetka Profesora Włodzimierza Żuka (1916 – 1981)

Stanisław Hałas

Zakład Spektrometrii Mas, Instytut Fizyki UMCS, plac Marii Curie-Skłodowskiej,

20-031 Lublin, e-mail: stanisł[email protected]

Profesor Włodzimierz Żuk urodził się 29.IX.1916 w Klimowiczach (obecnie teren Białorusi). Jego ojciec

wykładał matematykę w Seminarium Nauczycielskim w Siedlcach, matka pracowała jako nauczycielka. W

okresie I wojny światowej rodzina przemieszczona została w głąb Rosji. Włodzimierz Żuk w Siedlcach

ukończył 4 klasy Gimnazjum im. Żółkiewskiego, następnie 4 klasy ukończył w Gimnazjum im.

Zamoyskiego w Lublinie. Po maturze odbył służbę wojskową przez 1 rok w Wołyńskiej Szkole

Podchorążych Rezerwy Artylerii we Włodzimierzu Wołyńskim. Następnie studiował fizykę na

Uniwersytecie Warszawskim w latach 1936-1939. Magisterium uzyskał już po wojnie na UW, w roku 1946

na podstawie badań z fosforescencji kryształów u prof. Stefana Pieńkowskiego. Bardzo szybko, bo już w

1949 r. Włodzimierz Żuk zdobył stopień doktora nauk matematyczno-przyrodniczych na podstawie pracy

dotyczącej zjawisk jonizacyjnych w spektrometrze masowym.

W czasie kampanii wrześniowej 1939 r. Włodzimierz Żuk walczył w armii gen. Kleeberga,

uczestnicząc w słynnej bitwie pod Kockiem. Okres okupacji przebył w okolicach Białej Podlaskiej.

Natychmiast po wyzwoleniu Lubelszczyzny, bo już 1 września 1944 r. rozpoczął pracę, najpierw w Liceum

Chemicznym w Lublinie, a od listopada także na Uniwersytecie Marii Curie-Skłodowskiej. Przez pierwsze

dwa lata pracował na obydwu etatach, potem tylko na Uniwersytecie, gdzie przez niemal 37 lat zajmował się

fizyką eksperymentalną, przy czym prawie cały czas fizyką jądrową.

Na początku swojej kariery W. Żuk był asystentem prof. Jana Blatona i prof. Stanisława Ziemeckiego.

W bardzo szybkim tempie przebył dalsze szczeble kariery uniwersyteckiej pełniąc kolejno funkcje adiunkta,

zastępcy profesora, docenta, profesora nadzwyczajnego (1960). W roku 1967 został mianowany profesorem

zwyczajnym. Chociaż od 1944 r. przez cały czas W. Żuk związany był z UMCS, to jednak pracował

równolegle na etatach poza Uniwersytetem: w Liceum Chemicznym (1944–1946), w Zakładzie Fizyki

Cząstek Elementarnych w Warszawie jako kierownik Laboratorium Neutronowego przy budowie

pierwszego reaktora (1954–1955), w Instytucie Badań Jądrowych w Świerku (1955–1961), w Wyższej

Oficerskiej Szkole Lotniczej w Dęblinie. Wykładał także fizykę w byłej Filii UMCS w Zamościu.

Prof. Żuk wcześnie nawiązał kontakty naukowe z zagranicą, pierwsze już w listopadzie 1944 r. z

Uniwersytetem im. Łomonosowa w Moskwie. W latach 1946–1947 trzy razy wyjeżdżał na do Berlina, gdzie

wspólnie z prof. Stanisławem Ziemeckim dokonał zakupu aparatury naukowej dla potrzeb UMCS oraz dla

innych ośrodków w Kraju. W kolejnych latach nawiązał kontakty z Vinca Institute of Nuclear Sciences w

Belgradzie (Jugosławia), z Uniwersytetem Lajosa Kossutha w Debreczynie, Zjednoczonym Instytutem

Badań Jądrowych w Dubnej (ZSSR) oraz instytutami naukowymi w NRD, Szwecji i Danii. Z licznych

wyjazdów zagranicznych profesora wymieńmy te, które dla rozwoju fizyki jądrowej na UMCS miały



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54

szczególne znaczenie: w 1957 r. - półroczny staż naukowy w Instytucie Nobla w Sztokholmie, w 1961 r. - 9-

miesięczny pobyt na Uniwersytecie w Uppsali, w 1968 r. - w Instytucie Oersteda w Kopenhadze.

Zagraniczne staże pogłębiły jego wiedzę w tej dziedzinie i skłoniły do intensywnych prac nad budową

aparatury spektroskopii jądrowej, spektrometrów beta i gamma oraz aparatury do pomiaru korelacji

kątowych gamma-gamma i e-gamma. Profesor Żuk kierował pracami grupy lubelskich naukowców w

Zjednoczonym Instytucie Badań Jądrowych w Dubnej inicjując szereg badań dotyczących wyznaczania

wartości spinów stanów wzbudzonych i multipolowości przejść gamma w jądrach pierwiastków ziem

rzadkich.

Nawiązane wcześniej kontakty naukowe były stale przez prof. Żuka odświeżane, a także

nawiązywane nowe na międzynarodowych konferencjach naukowych, w których brał czynny udział.

Prace naukowe prof. Żuka i jego zespołu w zakresie elektromagnetycznej separacji izotopów,

spektrometrii mas i spektroskopii jądrowej spotykały się z dużym uznaniem fizyków polskich i

zagranicznych. Główny kierunek badań naukowych, którym jest nadal uprawiana w Lublinie spektrometria

mas, rozwinął prof. Żuk na początku swojej pracy naukowej. W 1949 r. zbudował pierwszy w Polsce

spektrometr mas. Również jako pierwszy w Polsce zastosował zbudowany pod jego kierunkiem

elektromagnetyczny separator izotopów do implantacji jonów do półprzewodników. Jest autorem monografii

„Spektrometria masowa” (PWN 1956) a także redaktorem i zarazem autorem większości rozdziałów

monografii „Spektrometria mas i elektromagnetyczna separacja jonów” (PWN 1980). Bibliografia prac

profesora liczy 205 pozycji (Wojnarowicz 1980, Biblioteka Główna UMCS). Wiele prac zostało

opublikowanych czasopismach zagranicznych i w materiałach konferencji międzynarodowych.

Prof. Żuk był od r. 1970 kierownikiem Zakładu Fizyki Jądrowej w Instytucie Fizyki. W przeszłości

pełnił wiele funkcji administracyjnych na Uniwersytecie: od 1956 r. pełnił funkcję kierownika Katedry

Fizyki Doświadczalnej, w latach 1960–1962 był dziekanem Wydziału Mat-Fiz-Chem, zaś w latach 1962–

1968 prorektorem do spraw nauki.

Był wychowawcą dwóch pokoleń fizyków – wykształcił ponad 300 magistrów, przeprowadził 19

przewodów doktorskich i kilka habilitacyjnych. Dla pracowników zakładu prof. Żuk był nie tylko

autorytetem naukowym, lecz również opiekunem i wychowawcą. Wymagający i krytyczny, gdy chodzi o

sprawy naukowe, jednocześnie z ogromną życzliwością pomagał w rozwiązywaniu trudności zarówno

naukowych, jak i życiowych. Codzienny kontakt z nim bardzo ułatwiała jego bezpośredniość i szczerość.

Zmarł nagle w pełni sił twórczych 13 stycznia 1981 r. Obszerny życiorys prof. Włodzimierza Żuka

opublikowali jego byli współpracownicy – prof. dr hab. Dariusz Mączka i dr Janusz Zinkiewicz (1982),

Postępy Fizyki, tom 33, 273-297.



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Contents

Pages

i Editorial pages

1 Preface

3 Program of Conference

5 FROM MS20 TO NU NOBLESSE: A SHORT STORY OF K-Ar DATING IN KRAKÓW

Michał Banaś

8 SHRIMP IIE/MC ION MICROPROBE

Zbigniew Jan Czupyt

11

METHODOLOGICAL ASPECTS OF K-Ar DATING IN APPLICATION TO

SEDIMENTARY BASINS THERMAL HISTORY RECONSTRUCTION

Sylwia Kowalska, Stanisław Hałas, Artur Wójtowicz, Claus Wemmer, Zbyszek Mikołajewski

14

HOW FAR WE CAN GET WITH HIGH-SPATIAL RESOLUTION GEOCHRONOLOGY

FOR U-PB DATING OF ANCIENT ROCKS

Kusiak M.A., Dunkley D.J, Lyon I. , Wirth R. , Whitehouse M.J., Wilde S.A.

16 FLUIDS ATTACK THE CITADEL OF ZIRCON: SOME CASE STUDIES

D. J. Dunkley, M. A. Kusiak, Y. Hiroi, K. Tani, D. E. Harlov , K. Shiraishi

19 CLUMPED ISOTOPES: THEORY, CALIBRATIONS AND APPLICATIONS

Sándor Kele

24 TOWARDS DETERMINATION OF MULTIPLE SULFUR ISOTOPE FRACTIONATION

S. Hałas, T. Pieńkos

26

STABLE S AND O ISOTOPES IN THE WIŚNIÓWKA ACID MINE DRAINAGE WATER

BODIES (HOLY CROSS MOUNTAINS, POLAND)

Zdzisław M. Migaszewski, Agnieszka Gałuszka

29

IMPROVED TRIPLE-FILAMENT ION SOURCE FOR TIMS USED IN 7Li/6Li AND

39K/41K RATIOS DETERMINATIONS

A. Pacek, T. Pieńkos, S. Hałas

33

MICROANALYSIS OF PGE MINERALS IN MONCHEGORSK PLUTON, KOLA

PENINSULA, BALTIC SHIELD

Huber M., Mokrushin A., Neradowski Yu., Halas S., Skupiński S.

36

INTERLABORATORY LUMINESCENCJE DATING OF MESO-PLEISTOCENE LOESSES

FROM WOŁYŃ AND PODOLE: METHODICAL ASPECTS

Stanisław Fedorowicz, Maria Łanczon , Andriy Bogucki, Karol Standzikowski ,

Przemysław Mroczek, Jarosław Kusiak

38

3.9 GA METAMORPHITE BLOCK FROM MURMANSK: MINERALOGICAL

CHARACTERISTICS

Huber M., Bayanova T.B. , Hałas S., Reszczyńska E., Lata L. , Skupinski S.



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41

IGNEOUS PROTOLITHS OF THE UIVAK GNEISS, PRELIMINARY DATA FROM THE

SAGLEK BLOCK, NORTHERN LABRADOR

Kusiak M.A., Dunkley D.J., Sałacińska A., Whitehouse M.J., Wilde S.A.

44

ENVIRONMENTAL AND POLLUTION CHARACTERISTICS OF THE LUBLIN

ROUGHCAST

Huber M. , Lata L.

46

ENVIRONMENTAL AND POLLUTION CHARACTERISTIC OF PLANTS SAMPLES

FROM KARKONOSZE REGION, S POLAND ROUGHCAST

Karpinski T.M., Huber M., Lata L

48

A DUAL INLET AND TRIPLE COLLECTOR MASS SPECTROMETER FOR ANALYSIS

OF 33S/32S AND 34S/32S ISOTOPE RATIOS

Pieńkos T., Hałas S., Pelc A., Wójtowicz A.

50

ENVIRONMENTAL MOSS CHARACTERISTICS FROM MIDDLE ROZTOCZE

(TOMASZÓW AREA)

Huber M. , Lata L.

52 FLUORINATION LINE FOR EXTRACTING OF OXYGEN FROM MINERALS

Ciszak A.

53 OUTLINE OF PROFESSOR WŁODZIMIERZ ŻUK (1916 – 1981) LIFE

Hałas S.



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Index of Authors

Banaś M. 5

Bayanova T.B. 38

Bogucki A. 36

Ciszak A. 52

Czupryt Z. J. 8

Dunkley D.J. 14, 16, 41

Fedorowicz S. 36

Gałuszka A., 26

Hałas S. 11, 24, 29, 33. 38, 48, 53

Harlov D.E. 16

Hiroi Y. 16

Huber M. 33, 38, 44, 46, 50

Karpiński T.M. 46

Kele S. 19

Kowalska S. 11

Kusiak J. 36

Kusiak M.A. 14, 16, 41

Lata L. 38, 44, 46, 50

Lyon I. 14

Łanczont M. 36

Migaszewski Z.M. 26

Mikołajewski Z. 11

Mokrushin A.V. 33

Mroczek P. 36

Neryadovskiy Yu. 33

Pacek A. 29

Pelc A 48

Pieńkos T. 24, 29, 48

Reszczyńska E. 38

Sałacińska A. 41

Skupiński S. 33, 38

Standzikowski K. 36

Tani K. 16

Wemmer C. 11

Whitehouse M.J. 14, 41

Wilde S.A. 14, 41

Wirth R. 14

Wójtowicz A. 11, 48

Documents

Geo-Science Education Journal - mahuber.commahuber.com/GSEJ_WWW/GSEJ2016_2(supl)Full issue.pdf · Geo-Science Education Journal 2016; 2 ... Fluids attack the citadel of zircon: